C B 



Water-Supply and Irrigation Paper No. 199 



Series I ^'STP^i^'J^l^^^'^l^ 
1 0, Underground Waters, 70 



DEPARTMENT OF THE I.N^TERIOR 

UNITED STATES GEOLOGICAL SURVEY 

CHARLES D. WALCOTT, Director 



UNDERGROUND WATER 



IN 



SANPETE AND CENTRAL SEVIER 
VALLEYS, UTAH 



BY 



G. B. RICHARDSON 




WASHINGTON 

GOVERNMENT PRINTING OFFICE 
1907 



-jr 



Class T 




Book U37i(p 



Water-supply and Irrigation Paper No. 199 Seriesj g; gX^J^^^^^^^^^ 



70 



DEPAETMENT OF THE INTERIOR 

UNITED STATES GEOLOGICAL SURVEY 

CHARLES D. WALCOTT, Director 



UNDERGROUND WATER 



12i 



IN 



SANPETE AND CENTRAL SEVIER 
VALLEYS, UTAH 



BY 



G. B. RICHARDSON 




WASHINGTON 

GOVERNMENT PRINTING OFFICE 

1907 



^\^ 



%^ 



MAR 31 1908 

D. or a 



CONTENTS. 



Page. 

Introduction 5 

Topography 6 

Geologj^ 8 

Bed rocks 8 

Jurassic system 8 

Cretaceous system 9 

Undetermined age 10 

Tertiary system __^ :. 10 

Igneous roclvs . 12 

Valley deposits 12 

Quaternary system 12 

Structure 13 

Source of underground water :: 14 

Precipitation : 15 

Flow of streams 16 

Other sources 21 

Distribution of underground water , : 21 

In bed rocks 22 

In valley deposits__ »_ 23 

Recovery of underground water 24 

From bed rocks 25 

By springs 25 

By tunnels s 26 

By wells 27 

From valley deposits 27 

By springs 27 

By tunnels. __■ 28 

By nonflowing wells 28 

By flowing wells 29 

By subsurface dams, etc 30 

Quality of water 30 

Suggestions 32 

Detailed descriptions 34 

Joseph and vicinity 34 

Elsinore and vicinity 35 

Monroe and vicinity 36 

Richfield and vicinity 37 

Salina and vicinity 40 

Gunnison and vicinity 42 

Mayfield and vicinity 43 

Manti and Ephraim 44 

Moroni and vicinity 46 

Fountain Green and Wak.:-__- 47 

Mount Pleasant and vicinity 48 

Well and spring data 51 

Index 61 

3 



ILLUSTRATIONS. 



/ Page. 

Plate i! A, Sagebrush upland south of Freedom, showing alluvial fan ; 

B, cultivated fields south of Ephraim 5 

II: Reconnaissance geologic map of Sanpete and central Sevier 

valleys Pocket 

III. Structural sections across Sanpete and central Sevier valleys-- 12 
IY/A, Fault spring west of Fountain Green ; B, the Wasatch 

monocline and M^iti Creek 14 

V. Map showing approximate depth to ground water and location 

of wells and springs^n central Sevier Valley 22 

VI. Map showing approximate depth to ground water and location 

of wells and springs in Sanpete Valley 24 

Fig. 1. Map of Utah, showing position of Sanpete and central Sevier 

valleys-^ 6 

2. Hypothetical section across Sanpete Valley 13 

3. Diagrammatic section at Richfield Spring - 26 

4. Diagrammatic section at Morrison Tunnel Spring 26 

5. Section illustrating a tunnel in the valley deposits. 28 

4 



U. S. GEOLOGICAL SURVEY 



WATER-SUPPLY PAPER NO. 199 PL. 




A. SAGEBRUSH UPLAND SOUTH OF FREEDOM, SHOWING ALLUVIAL FAN. 




B. CULTIVATED FIELDS SOUTH OF EPHRAIM. 



UNDERGROUND WATER IN SANPETE AND CENTRAL 
SEVIER VALLEYS, UTAH. 



By G. B. Richardson. 



INTRODUCTIOIS^. 

Sanpete and central Sevier valleys ate situated at the border of 
the Basin Range and Plateau provinces in south-central Utah. They 
are bounded on the east by the Wasatch and Sevier plateaus and on 
the west by the Gunnison Plateau and the Valley and Pavant ranges, 
and are drained by Sevier River, which empties into Sevier Lake in 
the Great Basin. (See fig. 1, p. 6.) 

These valleys rank with the richest parts of the State. They were 
occupied a few years after the Mormon pioneers founded Salt Lake 
City, in 1847, when settlements, which soon became thriving farm- 
ing communities, were established where water for irrigation was 
most available. A variety of crops, especially wheat, are success- 
fully grown, and the valleys are popularly known as the " granary 
of Utah." Sheep raising is also an important industry, the adjacent 
highlands being used for summer pastures. The climate is arid, and 
there is a striking contrast between those areas which in their natural 
state are covered with sagebrush and grease wood and the fruitful 
cultivated tracts. (See PL I, A and B.) Trees are normally absent 
in the valleys, but they flourish to a limited extent on the adjacent 
highlands, where there are thin growths of quaking aspen, scrub 
oak, and stunted conifers. Irrigation is necessary for the produc- 
tion of crops.* Canal systems are maintained by San Pitch Creek and 
Sevier River, and the mountain streams are tapped by ditches near 
the mouths of the canyons, but this supply is insufficient and atten- 
tion is being turned to the subterranean store. 

This report is a preliminary statement of the general conditions 
of occurrence of underground water in Sanpete and central Sevier 
valleys. The field work was carried on in cooperation with Sanpete 
and Sevier counties through the State engineer, Mr. Caleb Tanner, 
who detailed Mr. C. S. Jarvis to collect the data embodied in the list 
of springs and wells on pages 51-60. 

" Dry farming has not yet been extensively practiced here. 



6 UNDEEGEOUKD WATER IN VALLEYS OP UTAH. 

TOPOGRAPHY. 

Sanpete and central Sevier valleys are structural troughs filled 
with " wash " derived from the adjacent highlands. They trend 
northeast - southwest, and are Occupied by relatively small streams, 
Sevier River draining the southern, and its tributary, San Pitch 




Fig. 1.— Map of Utah, showing position of Sanpete and central Sevier valleys. 

Creek, the northern valley. Each valley is about 45 miles in length 
and averages 6 miles in width. 

The main central streams have a number of tributaries, the more 
important of which flow from the eastern plateaus, where the pre- 
cipitation is greater than on the relativel}^ low and narrow western 
highlands. The streams flow perennially within the mountains. 



TOPOGRAPHY. Y 

where they occupy steep, narrow valleys, but at the mouths of the 
canyons the discharge is largely diverted by irrigation canals, and the 
lower courses in the broad lowlands are generally dry, except during 
floods. The chief tributaries of San Pitch Creek are Cottonwood, 
Pleasant, Cedar, Oak, Canal, Ephraim, Willow, Manti, Sixmile, and 
Twelvemile creeks, all of which have small drainage areas on the 
Wasatch Plateau. Salina Creek, draining 255 square miles, is by far 
the largest tributary stream. It flows in the depression between 
the Wasatch and Sevier plateaus and joins Sevier Eiver 13 miles 
above Gunnison. The other important tributaries of the Sevier 
in its central valley are Lost and Monroe creeks, which rise in the 
Sevier Plateau. 

The elevation of Sanpete and central Sevier valleys ranges from 
5,000 feet above sea level in their lower parts to about 6,000 feet at 
the upper border of the lowlands, above which the mountains rise 
from 2,000 to 5,000 feet higher. 

Gunnison Plateau, bordering Sanpete Valley on the west and sep- 
arating it from Juab Valley, is 35 miles long and varies from 2 to 
8 miles in width. The plateau is considerably dissected, and only 
remnants of its former surface are preserved by horizontal beds of 
limestone. At its northern end the plateau has an elevation of almost 
10,000 feet, but it slopes southward and merges into Sevier Valley at 
Gunnison. A sparse growth of vegetation is supported on the Gun- 
nison Plateau, from which only a few feeble streams are tributary 
to Sanpete Valley. 

The Wasatch Plateau borders Sanpete Valley on the east and ex- 
tends as far south as the valley of Salina Creek. The crest of the 
plateau is underlain by Cretaceous and Tertiary sediments, which, on 
the east, form a wall of erosion, beyond which the surface slopes to 
Castle Valley, a lowland underlain by shale, which separates the 
plateau from the San Eafael swell. On the west the Wasatch 
Plateau slopes toward Sanpete Valley, conforming with a great 
monoclinal flexure. The Wasatch Plateau is comparatively well 
timbered and is the source of a number of perennial streams. 

Sevier Plateau forms the greater part of the eastern boundary 
of Sevier Valley, above which it rises abruptly, and extends from the 
valley of Lost Creek far to the south of tlxe area under consideration. 
Its culminating point is Monroe Peak, whose elevation is 11,240 
feet. The plateau is underlain by a series of igneous rocks, chiefly 
Tertiary tuffs and lavas. The East Fork of Sevier River receives a 
considerable part of the drainage of Sevier Plateau, but Monroe 
Craek is the only important stream that drains directly from it into 
the area here considered. 

Central Sevier Valley is bounded on the west by the Pavant and 
Valley mountains, which are the easternmost parts of the Basin 



» UNDERGROUND WATER IN VALLEYS OF UTAH. 

Ranges in this latitude. The Pavant Mountains are about 35 miles 
long and from 4 to 12 miles wide and are much dissected, their crest 
forming a narrow ridge about 10,000 feet in elevation. The range is 
but fairly well timbered and only a few small creeks flow from it to 
the valley. The eastern slopes are underlain by east-dipping strata, 
which unconformably overlie Paleozoic limestone. The Valley 
Mountains lie between the Gunnison Plateau and the Pavant Moun- 
tains, of which they are a faulted oifset. They are 25 miles long, 
average 5 miles in width, and are about 7,000 feet high. They are 
practically bare of vegetation and give rise to no important streams. 

GEOJLOGY. 

Sanpete and Sevier valleys are represented on the map of the 
Wheeler Survey " and are described in Dutton's report on the geolog;y 
of the High Plateaus of Utah,^ but no detailed geologic work has yet 
been done in this region. The character and structure of the rocks 
are fairly well known, however, and the following brief summary, 
together with the maps and sections (Pis. II, III, V, and VI), indi- 
cates the general geologic conditions of occurrence of underground 
Avater. 

The rocks of these valleys can conveniently be classified as con- 
solidated " bed rocks," which outcrop chiefly on the highlands, and 
unconsolidated deposits, which occur in the broad central valleys. 
Strata of Mesozoic and Tertiary age occupy the greater part of the 
highlands, and igneous rocks are found in their extreme southern 
portion. The valleys, on the other hand, are underlain to con- 
siderable depths by debris derived from the disintegration of the 
adjacent highlands. The underground water occurs chiefly in the 
unconsolidated deposits, but water contained in the bed rocks is 
locall}?- important. 

BED ROCKS. 
JURASSIC SYSTEM. 

So far as known, the oldest rocks of Sanpete and Sevier val- 
leys are of Jurassic age. They consist of a considerable but undeter- 
mined thickness of fissile clay shales, generally drab in color, but 
locally red, with some intercalated layers of drab sandstone ranging 
in thickness from a few inches to a few feet. Lenses of gypsum and 
rock salt are irregularly interbedded throughout the formation. 
These rocks outcrop in a range of low hills, about 30 miles long and 
2 miles wide, that extend along the eastern margin of Sevier Valley 
from Glenwood to the vicinity of May field. A less extensive outcrop 

« U. S. Geog. Surv. W. 100th Mer., Atlas. 

^ Dutton, C. E., Geology of the High Plateaus of Utah : U. S. Geog. and Geol. Surv. 
Rocky Mt. Region, 1880. 



JURASSIC AND CEETACEOUS EOCKS. \) 

occurs in the center of the valley, mostly west of Sevier River, be- 
tween Redmond and Gunnison. On the east a fault causes these 
Jurassic strata to abut against Tertiary beds, as mentioned later, 
but relations are generally concealed b}^ Quaternary deposits. The 
hills are practically bare of vegetation, and the soft beds have been 
eroded into badland topography. These rocks are of no value in 
the recovery of underground water. They exert, however, an impor- 
tant deleterious influence upon the character of streams with which 
they come in contact because of the ready solubility of their inter- 
bedded salt and gypsum. 

CRETACEOUS SYSTEM. 

The Cretaceous system is represented by two divisions, the Col- 
orado and the Laramie. A small outcrop of rocks of Colorado age 
occurs in the valley of Salina Creek just above the mouth of the 
canyon, about 3 miles from Salina. These are a thin-bedded buff 
sandstone, with subordinate drab shale carrying Inoceramus labia- 
tus.^ At the western limit of their outcrop the Colorado strata stand 
almost vertical and are directly overlain by horizontal Eocene beds. 
Because of their limited exposure these rocks also are unimportant 
in the recovery of underground water. 

Sandstones and shales provisionally referred to the Laramie divi- 
sion of the Cretaceous occupy a much greater area. The coal-bearing 
Laramie beds of Carbon County, which outcrop along the eastern 
scarp of the Wasatch Plateau, are conformably overlain by massive, 
loose-textured, buff sandstone, with subordinate interbedded buff shale. 
The thickness of these rocks has not been determined, but it amounts 
to several hundred feet.^ They locally cap the plateau and outcrop 
along its middle western flanks east of Sanpete Valley as far as 
Spring Creek, and are exposed farther south in the valleys of 
several creeks that have cut deeply into the Wasatch monocline. 

The only fossils that have been found in this formation on the 
Wasatch Plateau are a fcAV obscure fragments of leaves, but in what 
is probably the same formation, in a fault block south of Manti, in 
which the Sterling coal ^ occurs, a number of plant remains have been 
found. Among them F. H. Knowlton recognizes Sabalf cf. Saha- 
lites Grayanus^ Asimina eocenicaf Lesq., and Salix sp. ? From these 
he concludes that the formation is probably of Laramie age. 

At many localities on the Wasatch Plateau these rocks are overlain, 
apparently conformably, by Eocene strata. Different sections at the 
base of the knowm Tertiar}^, however, show deposits so diverse and 

« Determined by T. W. Stanton. 

^•Taff, J. A., Book Cliffs coal field, Utah : Bull. U. S. Geol. Survey No. 285, p. 292. 
<" Richardson, G. B., Coal in Sanpete County, Utah : Bull. U. S. Geol. Survey No. 285, 
p. 280. 



10 UNDEKGROUND WATER IN VALLEYS OF UTAH. 

thicknesses so different that there is no conformity in the sense of a 
succession of widespread, uniform, uninterrupted deposits. In the 
vicinity of Sterling a distinct local unconformity is marked by flat 
Tertiary beds resting on highly inclined Laramie (?) sandstone. 

The sandstone on the flanks of the Wasatch Plateau is a probable 
source of artesian water. (See p. 22.) 

UNDETERMINED AGE. 

A considerable thickness of red and buff conglomerate and sand- 
stone, amounting to at least 2,000 feet, is exposed on the eastern 
flanks of the Pavant Mountains and Gunnison Plateau! The con- 
glomerate is composed of rounded pebbles of quartzite and subordi- 
nate limestone of variable size, up to 1 foot in diameter, embedded 
in a sandy matrix. The main mass of conglomerate is overlain by 
fine-textured sandstone, but intercalated with the sandstone there are 
also beds of conglomerate. Drab shale of minor importance is locally 
interbedded with the sandstone. In the valley of upper Corn Creek, 
about 8 miles northwest of Elsinore, the basal conglomerate rests upon 
the eroded surface of steeply tilted Paleozoic sediments, and a simi- 
lar conglomerate overlies upturned Carboniferous strata at the east- 
ern base of Mount Nebo, about 15 miles northwest of Fountain 
Green. These conglomerates and sandstones, both on the Gunnison 
Plateau and on the Pavant Mountains, are overlain in apparent con- 
formity by strata of Eocene age, but no fossils have been found in 
either the conglomerate or the sandstone, and the age of the rocks is 
as yet undetermined. The disconnected areas that have the same 
color on the map are grouped together only provisionally. 

^he conglomerate sandstone formation on the eastern flank of the 
Pavant Mountains is likely to prove a source of artesian water. 
(See p. 23.) 

TERTIARY SYSTEM. 

Strata of Eocene age outcrop on the summit and western flanks of 
the Wasatch Plateau, on the summit and eastern part of the Gunni- 
son Plateau, and on the eastern slope of the valley and Pavant Moun- 
tains, and also form low ridges in Sevier and Sanpete valleys. These 
Tertiary sediments consist of at least 2,000 feet of drab, green, and 
red shales, buff and reddish sandstones, and whitish, fresh-water 
limestones. The stratigraphy is varied, and even adjacent sections 
are rarely alike. Numerous fresh-water fossils, including Sphmrium^ 
Planorhis^ Pliysa^ Goniohasis^ and Vivipara,^ occur in these rocks, 
which are referred to the Wasatch stage of the Eocene. The fol- 
lowing section was measured west of Wales. 

« Identified bv W. H. Call. 



TERTIARY ROCKS. 11 

Generalized section of Eocene rocks on Gunnison Plateau icest of Wales. 

Feet. 

Fine-textured white limestone lOO-f 

Interval of talus 100 

Gray limestone 10 

Brown sandstone 10 

Interval of talus 150 

Brown sandstone 5 

Drab limestone ]."> 

Brow^n sandstone 10 

Drab limestone 5 

Interval of talus 100 

White limestone 10 

Drab shale 50 

Buff limestone __- 15 

Drab shale 50 

Interval of talus 350 

Drab limestone 10 

Drab shale with streaks of purple shale 150 

Brown sandstone 20 

Drab shale with few thin beds of limestone 250 

Brown sandstone 5 

Drab shale 25 

Brown sandstone 10 

Buff shale 100 

Gray limestone 25 

Black limestone 5 

Coal and bone 7 

Black limestone 10 

Dark shale 15 

Brown sandstone 10 

]>rab shale 10 

Gray limestone 5 

Buff shale 40 

Sandstone 10 

The coal noted above is locally important, « but is not of widespread 
occurrence. 

Younger Eocene strata outcrop in low ridges in Sanpete Valley, 
extending northward from Manti. They dip westward at low angles 
and their outcrops are surrounded by Quaternar}^ deposits which con- 
ceal relations with the underlying rocks exposed on the flanks of the 
adjacent plateau. These j^ounger rocks consist of light-colored sand- 
stone, shale, and limestone, including a bed of oolitic limestone, and 
contain well-preserved specimens of fishes, turtles, etc. Cope '^ named 
them the Manti beds and regarded them as middle Eocene, corre- 
sponding to the AVind River stage. Because of insufficient knowl- 
edge concerning the base of the formation it is not differentiated here, 

" Richardson, G. B.. Coal in Sanpete County, Utah : Bull. U. S. Geol. Survey No. 
285, p. 292. 

*Cope, E. D., The Manti beds : Am. Naturalist, vol. 14, 1880, p. 303. 



12 UNDERGROUND WATER IN VALLEYS OF UTAH. 

but is mapped as Eocene, together with the strata referred to the 
Wasatch stage. 

The varying stratigraphy^ of Eocene strata, the prevalence of 
shale and limestone, and the minor occurrence of more pervious 
strata render the rocks of little importance as water reservoirs. Yet 
these relatively impervious beds serve to confine water in the under- 
lying sandstones and conglomorates, and are thus important factors 
in the occurrence of artesian water. 

IGNEOUS ROCKS. 

Igneous rocks are unimportant as water reservoirs in Sanpete and 
Sevier valleys, for they occupy small areas and are massive, fine 
textured, and of low porosity. Their occurrence is chiefly restricted to 
the upper part of central Sevier Valley, to the Sevier Plateau south 
and east of Richfield, and to the base of the Pavant Range, west of 
Elsinore. They constitute the northern end of a mass which is well 
developed farther south. These rocks are for the most part a com- 
plex series of lavas that were poured out upon eroded surfaces of 
the underlying strata at different intervals in Neocene time.'* 

VALLEY DEPOSITS. 

QUATERNARY SYSTEM. 

The broad central floor of Sanpete and Sevier valleys is composed 
of fine-textured soils, chiefly sand and clay loam, but toward the 
highlands the material becomes coarser and the mountains are flanked 
by alluvial fans and slopes consisting of sand and gravel, with sub- 
ordinate clay, the coarser material preponderating near the moun- 
tains. These deposits are derived from the disintegration of the 
adjacent highlands and transported to the valley by streams. In 
their mountain courses the volume and velocity of the creeks are con- 
siderable, especially during floods, and their carrying power is pro- 
portionally large, but upon entering the valley both volume and 
velocity decrease, the result being that the coarser materials carried 
by the streams are dropped near the base of the highlands while the 
finer debris is borne farther into the lowlands. Alluvial fans, con- 
sisting of heterogeneous masses of coarse sand and gravel, are thus 
formed about the mouths of the canyons (PL I, A), and alluvial 
slopes accumulate along the base of the mountains between the creeks, 
chiefly as the result of torrential storms. 

The deposits beneath the surface of the broad valleys consist of 
gravel, sand, and clay, the thickness of which is considerable, but 

« Button, C. E., Geology of the High Plateaus of Utah : U. S. Geog. and Geol. Surv. 
Rocky Mt. Region, 1880. 



U. S. GEOLOGICAL SURVEY 





I.Jurassic? 2. Colorado 3. Laramie ? 



STRUCTURAL 




STRUCTURAL SECTIONS ACROSS SANPETE AND CENTRAL SEVIER VALLEYS 



STRUCTURE OF THE ROCKS. 



13 



unknown; minimum depths in the main part of the valleys are 530 
feet in Sevier and 650 feet in Sanpete Valley, as shown by two Avells,'^ 
in neither of which was consolidated rock found. 
Alternating beds of gravel, sand, and clay, from 
a fcAV inches to many feet in thickness, are en- 
countered in driving wells. Few records have 
been kept, however, and the detailed underground 
distribution of the valley deposits remains to be 
determined. In general, coarse material prepon- 
derates near the highlands and finer textured 
debris is more abundant in the lowlands, the incli- 
nation of the deposits being toward the valleys, in 
the attitude of deposition. Sections, even of neigh- 
boring wells, can rarely be correlated, which im- 
plies that the deposits, instead of having wide 
lateral distribution, as homogeneous beds, consist 
of series of lenses, w^ith imperfect connection, as 
illustrated in the section forming fig. 2. These 
deposits are in large part loose, porous, and satu- 
rated with water, and constitute the most import- 
ant underground reservoirs of the region. 

STRUCTURE. 

The strata that cap the highlands lie practically 
flat, but have been tilted and faulted along the mar- 
gins of the lowlands, and the central valleys are 
structural depressions. The rocks are not folded 
in the strict sense of the term, but incident to the 
uplift of the plateaus monoclinal flexures and 
normal faults have been developed. (See PL III.) 

A conspicuous structural feature of the region 
is the monocline that marks the western border 
of the Wasatch Plateau. Near the rim of the 
plateau the strata dip westward, and along the 
flanks a dip slope of large proportions is devel- 
oped. (See PL IV, B.) On this the strata that 
outcrop on the summit descend between 4,000 and 
5,000 feet in about 5 miles and pass beneath the 
valley floor. Other large monoclines appear on 
the flanks of the Pavant and Valley ranges, where 
strata that dip eastward at a low angle descend 
toward Sevier Valley. The Jurassic shales that 
outcrop in a narrow belt between Glenwood and Mayfield constitute 







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« Nos. 101a and 186, pp. 53 and 55. 



14 UNDERGROUND WATER IN VALLEYS OF UTAH. 

another conspicuous zone of tilted strata. Throughout their extent 
they dip eastward at an average angle of 45°. 

One of the prominent faults in the area under consideration 
intersects the eastward-dipping strata of the Pavant Mountains at 
the base of the range. This fault extends along the border of the 
valley to a point about 8 miles north of Richfield, where it turns 
northwestward and causes the Eocene shales and limestones to abut 
against the underlying upthrown red conglomerates. 

The abrupt rise of Sevier Plateau several thousand feet above the 
valley and the presence of springs along its base indicate a fault, and 
a number of displacements that can be traced east of the valley and 
parallel to it lie between Glenwood and Manti. The eastward- 
dipping shales there form an upthrust block bounded on the east and 
west by north-south trending faults, by which the Jurassic beds are 
brought into contact with Eocene strata. The northern end of this 
block adjoins a much-disturbed zone between Mayfield and Manti, 
where the area between the Gunnison and Wasatch plateaus has been 
broken by several approximately parallel faults, as shown by the 
map and sections. The southwestern flank of the Wasatch Plateau 
is traversed by a number of minor parallel displacements, Avhich fade 
away to the north and have not been traced beyond Manti Creek. 
Along the eastern base of the Gunnison Plateau a fault brings the 
red conglomerate with a high eastward dip against practically hori- 
zontal Eocene limestones and shales. The throw of some of the 
faults is considerable, but data are lacking for close measurement. 

These structural features have an important bearing on the occur- 
rence of underground water, as described on pages 25-27. A number 
of strong springs are associated with the faults, and the monoclinal 
flexures control the occurrence of water under pressure. 

SOUKCE OF UNDERGROUIS^D WATER. 

The underground water supply of Sanpete and Sevier valleys is 
derived from the rain and snow that fall on their drainage areas. 
Of the total precipitation, part evaporates, part flows off in streams, 
and part sinks into the ground. The relative amounts that are thus 
disposed of vary greatly under different conditions, and a complex 
series of changes ensues between precipitation and the final disappear- 
ance of the Avater from the drainage basin. Evaporation occurs either 
directly — from snow, from a free surface of water, and from water 
contained in soils — or indirectly, by transpiration through the growth 
of plants. Of the portion of the precipitation that joins the run-off', 
part leaves the basin in surface streams and part is absorbed by the 
soils and rocks over which the streams flow. The underground sup- 
ply is further augmented by direct absorption from the surface on 



U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 199 PL. IV 




A. FAULT SPRING WEST OF FOUNTAIN GREEN. 




B. THE V/ASATCH MONOCLINE AND MANTI CREEK. 



SOURCE OF UNDERGROUND WATER. 



15 



which the rainfall occurs. Part of the subterranean waters find 
their way back to the surface in springs, another part is consumed 
by the groAvth of organisms and by mineralogical changes, and a 
third part joins the more permanent supply of underground water. 



PRECIPITATION. 

Precipitation on the highlands, especially snow, which falls early 
and lingers late, is the chief source of supply of the streams which, 
as will presently be shown, are the most important contributors to 
the store of underground water in the valleys. There are no records 
of precipitation on the highlands, but the marked difference in vege- 
tation between the forested mountains and the naturally desert 
valleys implies a considerably greater amount on the former. In the 
valleys, on the other hand, rainfall data have been kept for a number 
of years, although this precipitation contributes relatively little to 
the supply of underground water. 

The mean annual amount for the past seven years ranges from 
6.73 inches at Richfield to 11.37 at Mount Pleasant, and of this about 
40 per cent falls during January, February, and March, when the 
frozen condition of the ground is unfavorable for absorption. Be- 
sides the direct run-off, much of the precipitation in the valley joins 
the streams as seepage run-off, and, in addition to the water that is 
lost through plant growth, large amounts are evaporated from the 
ground, the supply being maintained by capillary action. A con- 
siderable part of the rainfall on the valley is therefore lost by run-off 
and evaporation. The remainder replenishes the more permanent 
supply of underground water, relatively large quantities being 
absorbed by areas that are underlain by porous sand and gravel. 

The following tables of precipitation at Richfield, Manti, and 
Mount Pleasant, compiled from records of the United States Weather 
Bureau, show the amount and distribution of the valley rainfall for 
the past seven years : 

Monthly and annual precipitation at Richfield from 1899 to 1905. 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 


Dec. 


Annual. 


1899 


0.30 
.45 
.60 
.35 
.60 
.55 
.90 


0.55 
.20 

".'65" 

".'26' 
1.66 


4.65 



1.07 

1. 35 

.57 

.16 


0.70 

'".■'23' 
.17 

'".'67 


T. 

0.08 

.10 

.32 

1.89 

1.03 


0.14 
T. 
.07 
.24 
T. 
.80 


0.10 

.14 
.18 
.31 
.27 


0.12 
.07 
.03 
.22 
.30 
.37 


0.07 

.07 



.64 

1.00 
.05 


0.88 
.05 


0.20 
.30 


1.05 

.74 
.47 
.04 
.80 
.28 


8.32 


1900 




1901 




1902 

1903 


.26 
.83 
.95 


1.77 

"'6' 


6.62 


1904 

1905 


5.25 


















i 




Mean 


.54 


.65 


1.56 


.29 


.58 


.31 


.21 


.19 


.37 


.49 


.76 


.56 


6.73 



16 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



Monthly and annual 


precipitation 


at Manti 


from 


189^ 


to 1905. 




Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 


Dec. 


Annual. 


1899 


1.90 
.61 
.02 
.52 
.73 

1.10 
.85 


2.00 
.25 
2.50 
.90 
1.18 
1.13 
3.42 










1.02 

.22 
.26 
.53 
.61 
T. 


1.13 


T. 


2.38 

-.60 

1.05 

.40 

1.21 

.94 

.54 


0.31 
.80 
.50 

1.38 

.20 



2.99 


1.30 



.55 

.86 

.40 

1.50 

1.10 




1900 


0.10 
1.00 
1.50 
1.16 
1.71 
1.90 







0.15 
.04 
.28 
.40 
.05 




1901 


0.80 
1.08 
1.22 
.93 
1.54 


1.00 
.49 
2.20 
2.03 
2.25 


1.23 
T. 
.11 
.37 
.20 


0.08 
.83 
.98 
.48 

3.09 


9.10 


1902 


8 26 


1903 


10.26 


1904 


11 20 


1905 


17.93 






Mean 


.82 


1.63 


1.23 


1.11 


1.59 


.18 


.53 


.61 


1.09 


1.02 


1.03 


.95 


11.35 



Monthly and annual precipitation at Mount Pleasant from 1899 to 1905. 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 


Dec. 


Annual. 


1899 


1.40 
.36 
.56 
.52 
1.24 
1.10 
.80 


3.60 
.60 
2.16 
.90 
1.10 
1.71 
1.93 


2.29 
.10 
2.37 
1.50 
1.40 
2.20 
1.76 


0.57 
2.56 
.13 
1.08 
1.41 
1.12 
1.47 


1.02 

.32 

.58 

.49 

1.49 

2.11 

1.25 


0.99 

.29 
.04 
.59 
.76 



0.76 
T. 
.19 
.26 
.56 

1.12 
.17 


1.24 

.16 
1.64 

T. 

T. 

.44 




1.78 

.16 

.83 

1.57 

.36 


1.80 
,59 

1.32 
.40 

.58 

.88 




0.88 
1.56 

.67 
1.38 

.20 



1.15 


2.10 
T. 

1.14 
.86 
.20 

1.90 

1.10 


16.65 


1900 


8.03 


1901 


11.21 


1902 


8.26 


1903 


10.34 


1904 


13.70 


1905 












Mean 


.85 


1.71 


1.66 


1.19 


1.03 


.53 


.51 


..87 


.94 


.93 


.97 


1.22 


11.37 



FLOW OF STREAMS. 



The streams of Sanpete and Sevier valleys are of three distinct 
types — the relatively long master streams, the shorter transverse 
tributaries, and the canals. The master streams, as already stated, 
meander in a gentle grade in broad waste-filled valleys of structural 
origin. San Pitch Creek, which is confined to the northern valley, is 
fed by the direct but varying flow of its tributary streams and by 
more constant seepage. Sevier River, on the other hand, while hav- 
ing similar sources of supply within the portion of its valley under 
consideration, is fed chiefly from sources in the high plateaus in the 
southern part of the State. 

The tributary streams are very different. In their mountain 
courses they occupy narrow, steep-graded, eroded valleys, and at the 
base of the highlands they emerge from their canyon-like courses 
and enter the broad debris-filled lowland, across which they flow at 
a lessened grade until they join the master stream. These tributary 
streams are fed almost entirely by the precipitation on their moun- 
tain watersheds through direct and seepage run-off, and as the main 
precipitation on the mountains occurs as snow, the discharge is 
heaviest in late spring and early summer. Figures are not available 
to show the run-off of the streams in the area under discussion, but 
the streams in Jordan Valley under similar conditions discharge 
during April, May, and June about 60 per cent of the annual run-off. 
Besides the annual floods, occasional violent summer storms tempo- 
rarily increase the discharge of the streams. Conditions are differ- 
ent in each watershed, the discharge varying with the precipitation, 



STREAM FLOW. 



17 



topography, vegetation, and soils, and with the care that is taken 
to prevent fires, excessive grazing, and the destruction of timber. 
Seepage run-off is greater in valleys of relatively low relief that are 
abundantly clothed with vegetation, for under these conditions the 
products of rock disintegration are not readily washed into the 
valleys, and debris accumulates to absorb a large quantity of the 
precipitation, which thus escapes flood discharge and seeps slowly 
into the streams, maintaining their perennial flow. Below the 
mouths of their canyons the tributary streams, in the upper parts of 
their way across the broad valley, receive no augmentation to their 
flow, but, on the contrary, lose much by evaporation and absorption, 
which will presently be referred to, while in their lower courses, 
before they enter the main streams, their flow is generally increased 
by seepage. During the irrigation season the tributaries make small 
contribution directly to the master streams, for their water at the 
mouths of the canyons is diverted by canals and distributed over the 
valley. 

Irrigation canals tap both master streams and tributaries, the 
tributaries at or near the mouths of the canyons, and San Pitch Creek 
and Sevier River at intervals throughout their courses, as shown 
on the map. Water is thus distributed over the valley where nor- 
mally it w ould not flow. 

The amount of water contributed by streams to Sanpete and Sevier 
valleys has not been measured. An indication, however, of the dis- 
charge of the most important ones is afforded by the following 
measurements, made with a current meter by C. S. Jarvis during 
the summer of 1905, but it must be borne in mind that at the time 
when most of the data were collected the streams were at a low stage. 
Discharge measurements of streams in Sevier and Sanpete valleys in 1905. 



stream, with place of measurement, a 


Date. 


Discharge. 


Sevier River above Clear Creek 


June 17 
do 


Sec.-ft. 
310 4 


Sevier River near Gunnison & 


51 




June 29 
do 


269.4 


Sevier River near Gunnison b 


17 


Clear Creek at mouth 


June 17 
June 29 
July 11 
Aug. 4 
Aug. 3 
Aug. 10 


119.2 


Do 


48.2 


Monroe Creek 


9 3 


Lost Creek 


6.3 


Salina Creek 


18.0 


Willow Creek 


1 1 


Twelvemile Creek 


30.7 


Sixmile Creek 


Aug. 17 
Aug. 19 
Aug. 30 
Sept. 16 
Sept. 18 
Sept. 19 
do 


16.5 


Manti Creek 


13.6 


Ephraim Creek 


8 3 


Canal Creek 


3.5 


Oak Creek 


4 8 


Cedar Creek 


1.5 


Twin Creek 


8 1 


Pleasant Creek 


do... 


8.3 


North Creek 


do 


1 6 


Cottonwood Creek at Fairview 


Sept. 22 


4.1 







» If locality is not stated, the stream was measured at or near the mouth of its canyon. 
* Estimated from gage reading. 

IRR 199—07 M 2 



18 



TJNDERGEOTJND WATER IK VALLEYS OF UTAH. 



Although the quantity of water tributary to Sanpete and Sevier 
valleys is not known, the amount that leaves them by San Pitch 
Creek and Sevier River near Gunnison has been measured for the 
last five years and is shown by the following tables, compiled from 
records of the United States Geological Survey: 

Estimated discharge of San Pitch Creek near Gunnison. 



Date. 


Discharge in second-feet. 


Total in 


Maximum. 


Minimum. 


Mean. 


acre-feet. 


1905. 


15 
24 
15 
94 

338 

304 

166 

720 

82 

46 

35 

30 


11 
9 
8 
13 
82 
90 
110 
64 
30 
26 
22 
20 


13.3 

14.1 

12.1 

24.2 

136.0 

179.0 

143.0 

126.0 

40.5 

32.0 

28.1 

23.9 


818 


February - . 


783 




744 


April 


1,440 


May ' 


8,362 


June 


10, 650 


July 


8,793 

7,747 




September 


2,410 


October 


1,968 




1,672 


December 


1,470 




Total 


338 


8 


64.3 


46,860 




1904 


264 
158 
155 
125 


6 
3 

7 
9 


43.7 
37.3 
27.0 
30.0 


31, 920 


1903 


27, 184 


1902 


19, 855 


1901 . . 


21, 803 







Estimated discharge of Sevier River near Gunnison. 



Date. 


Discharge in second-feet. 


Total in 


Maximum. 


Minimum. 


Mean. 


acre-feet. 


1905. 
January 18 31 


319 

573 

367 

92 

651 

525 

26 

69 

62 

101 

95 

116 


254 
254 
87 
41 
41 

]l 

24 
41 
58 
87 
93 


303.0 

318.0 

199.0 

67.0 

222.0 

164.0 

18.4 

32.3 

46.2 

89.3 

91.4 

98.3 


8,414 




17, 660 


Marcli 


12, 240 


April 


3, 987 


May . . 


13, 650 




9, 759 


July 


1,131 




1,986 


September 


2,749 


October 


5,491 




5.439 


Decem.ber 1-15 


2,925 






Total 


651 


17 




95, 009 








1904 


355 
366 
194 
239 


10 

8 
5 
5 


81.1 


58, 490 


1903 . 


73, 000 


1902 


54.0 
56.0 


38. 677 


1901 a 


40, 481 







a Five days missing in this year. 

If the figures for 1905 represent normal conditions, the flood dis- 
charge of San Pitch Creek occurs in May and June, the maximum 
occurring in June, after which the flow gradually decreases to the 
period of low water in January, February, and March, the minimum 
occurring in March. By comparing the total discharge of San Pitch 
Creek for the last five years it appears that the floAV is irregular, the 
discharge in 1905 being more than double that in 1902. The flow of 



STREAM FLOW. 19 

Sevier River, which drains a much larger area, is even more irregu- 
lar. In 1905 the maximum occurred in February, and the discharge 
in May was large, while the minimum occurred in July and August. 
The annual discharge varies considerably and in the dry year of 1902 
was less than half that in 1905. The flow of Sevier River is much 
affected by irrigation, return seepage, and absorption, as is shown by 
the fact that on June IT, 1905, the discharge of the river below Clear 
Creek, at the head of central Sevier Valley, was 429.6 second-feet, 
while 45 miles below, at Gunnison, the discharge amounted to only 51 
second-feet. Similar results were obtained on June 29. 

Although figures are lacking for estimating the quantity of water 
available for replenishing the underground store from the flow of 
streams, the data given below indicate that the amount is considerable. 
Absorption from stream beds is, in fact, the chief source of under- 
ground water in Sanpete and Sevier valleys. 

A few measurements to illustrate the amount of water absorbed 
from individual streams in parts of their courses were made by C. S. 
Jarvis in the summer of 1905, as follows : 

Ephraim Creek on August 30, flowing 8.2 second-feet near the 
mouth of its canyon, in a course of 0.6 mile over a gravelly bed lost 
0.8 second- foot, amounting to 16 per cent a mile. 

Oak Creek on September 18, flowing 4.88 second-feet at a point 3 
miles southeast of Spring City, in a course of 2.5 miles lost 0.46 
second-foot, amounting to 3.T per cent a mile. 

Twin Creek on September 19, flowing 8.1 second-feet at a point 
3.5 miles southeast of Mount Pleasant, in a course of about 2.T5 miles 
lost 3.1 second-feet, amounting to 13.8 per cent a mile. 

Moroni upper canal on September 12, flowing 6.38 second-feet, in 
a course of 7 miles lost 1.76 second-feet, amounting to 3.8 per cent a 
mile. 

These figures clearly indicate the manner in which the under- 
ground supply is maintained by streams. 

An instructive example of the role played by seepage is afforded 
by the flow of Sevier River between the mouth of Clear Creek and 
Gunnison, a distance of 45 miles. At three places between these 
points dams have been constructed across the river, and at each place 
canals divert practically all of the flow of the stream, yet below each 
dam the seepage into the river is sufficient to supply the next suc- 
ceeding canals. This fact is illustrated by the following measure- 
ments made by Caleb Tanner in 1902, which show that between 
Clear Creek and Rocky Ford the flow of the river was augmented 
through seepage by 26.06 second-feet, between Rocky Ford and Red- 
mond Ford by 18.2 second-feet, and between Redmond Ford and 
West View Bridge by 22 second- feet. 



20 UNDEKGROUND WATER IN VALLEYS OF UTAH. 

Seepage in Sevier Valley between Clear Creek and Gunnison.a 

[Measurements made by Caleb Tanner, August 13-16, 1902.] 

BETWEEN CLEAR CREEK AND ROCKY FORD. 

Surface water entering Sevier Valley : Sec. ft. 

Sevier River above Clear Creek 47.5 

Clear Creelv 7.3 

Monroe Creek 3.9 

Thompsons Creek .2 

Redbutte and Cottonwood creeks ., .3 

Water Canyon Creek .3 

Spring Creek 5.3 

Cove Creek 9.5 

Cedar Ridge Creek .5 

— 74.8 

Surface water diverted from Sevier Valley : 

Clear Creek canal 1.38 

Joseph canal 3. 85 

Wells canal 2.38 

Isaacson canal 3. 03 

Monroe canal 7.25 

Elsinore canal 2. 75 

Brooklyn canal ^_ 5. 50 

Richfield canal 17. 50 

Annabelle canal 11. 18 

Candor canal .50 

Vermilion canal 9. 04 

Surface water leaving valley : 

Sevier River ^ 36.5 

Total diverted and remaining in stream 100. 86 

Seepage 26. 06 



BETWEEN ROCKY FORD AND REDMOND FORD. 

Surface water entering Sevier Valley : 

Sevier River at Rocky Ford 36.5 

Lost Creek ^ .7 

Salina Creek 7.8 

45. 

Surface water diverted from Sevier Valley : 

Rock Ford canal 35.0 

Other canals 8.5 

Surface water leaving valley : 

Sevier River 19. 7 

Total diverted and remaining in stream 63.2 



Seepage 18. 2 



Water Sup. and Irr. Paper No. 85, U. S. Geol. Survey, 1903, pp. 91-94. 



SOURCE OF UNDERGROUND WATER. 21 

BETWEEN REDMOND FORD AND WEST VIEW RIDGE, . 

Surface water entering Sevier Valley : Sec. ft. 

Sevier River at Redmond Ford 19.7 

Willow Creek .5 

San Pitch Creek 15.2 

— 35.4 

Surface water diverted from Sevier Valley : 

Robbins canal 1 8.14 

Westview canal 4. 20 

Other canals 15. 70 

Surface water leaving Sevier Valley : 

Sevier River 18. 7 

Dover canal 10. 7 

Total 57. 44 

Seepage 22. 04 

OTHER SOURCES. 

The undergrown water-supply of Sanpete and Sevier valleys is 
augmented not only by rainfall that is directly absorbed by the sur- 
face on which it falls and by absorption from creek beds, but also 
by the flow of springs from bed rock, by the return waters of irri- 
gation, and by the underflow from the creeks at the mouths of their 
canyons. 

The occurrence of springs is described on pages 25-26, but it should 
be noted here that, in addition to many seeps, a number of springs that 
issue along fault lines convey water to the valley from a distant 
source in bed rock. The total discharge of these fault springs 
amounts to a constant flow of about 95 second-feet, and absorption 
of a part of the flow adds an appreciable amount to the underground 
waters. 

In the practice of irrigation part of the water applied to the fields 
is absorbed by the soil and, percolating below the reach of roots and 
beyond the sphere of capillary action, joins the underground supply. 
The amount thus absorbed varies considerably from place to place, 
depending on the porosity of the soil and the quantity of water 
applied to the fields in excess of the need. 

The underflow of the creeks at the mouths of their canyons also 
contributes an important quota to the underground supply of the 
valleys. No data are available to show this amount, but it can be 
determined by measuring the cross-section of the valley filling, its 
porosity, and the velocity of the underflow. 

DISTRIBUTIOK OF UNDERGROUND WATER. 

Underground water, derived from the sources that have been 
stated, is contained in both the unconsolidated deposits and the bed 
rocks of Sanpete and Sevier valleys. The former are the more valu- 



22 UNDERGROUND WATER IN VALLEYS OF UTAH. 

able reservoirs, but some of the consolidated deposits also are im- 
portant. All rocks, even the most dense, are to a certain extent 
porous, and the great mass of underground water is contained in rock 
pores and interstices. Fine-textured, compact deposits are relatively 
of little importance as water carriers, the chief reservoirs being the 
loose-textured, more permeable rocks. 

WATER IN BED ROCKS. 

As has been indicated in the preceding description of the rocks of 
this region, the general character of several of the formations ren- 
ders them of little value as underground reservoirs. The massive, 
fine-textured igneous rocks, except locally, where they are cracked, 
are practically worthless in this connection; so, too, are the Jurassic 
shales. The strata of known Eocene age, which occupy a large area, 
composed as they are of close-grained shale and limestone and thin 
lenses of sandstone, have also little value for absorbing and trans- 
mitting water. On the other hand, the sandstone of probable Lara- 
mie age that outcrops on the Wasatch Plateau and the conglomerate 
and sandstone of undetermined age on the Pavant Mountains are 
probably important water-bearing beds, although they have not been 
developed. These porous strata are of considerable thickness and 
outcrop on large areas in the mountains where the opportunities for 
absorption are good. They are overlain by relatively impervious 
beds and dip toward the valley. The conditions for obtaining ar- 
tesian water in the valleys are therefore favorable, except where 
there are disturbing factors, presently to be stated. 

The geologic map and sections (Pis. II and III) show that the 
Laramie sandstone occupies many square miles on the summit and 
western flanks of the Wasatch Plateau east of Sanpete Valley, ex- 
tending as far south as Salina Creek, and that toward the base of the 
plateau the sandstone is capped by shales and limestones of Eocene 
age. The dip is westward — toward the valley — at angles ranging 
from 5° to 20°. At the base of the highlands, however, the rocks are 
concealed by unconsolidated deposits, and little information is avail- 
able concerning the position of bed rock beneath the valley filling. 
At the southern end of. the Wasatch Plateau the western flank is 
broken by several north-south trending faults, which fade away 
northward, and none are known to extend beyond Manti Creek. No 
evidence of faulting at the base of the plateau has been obtained in 
the northern and central parts of Sanpete Valley, where the rocks 
that are exposed along the flanks of the plateau probably continue 
unbroken beneath the valley nearly to its western limit. The west- 
ern dip, if continued beneath the valley at the same angle, would 
carry the water-bearing beds beyond the reach of profitable drilling, 



rej'er to lists of wells and springs) 



Scale 
2 3 4 



6 milefi 



AND SPRINC^S 




MAP SHOWING APPK<)XIJIATE DEPTH TO GROUND WATERS AND LOCATTON OP WELI.S AM' SP81 
IN CENTRAI, SEVIER VALLEY UTAH 



DISTRIBUTION OF UNDERGROUND WATER. ^B 

but the rocks in the ridge between Fountain Green and Mount 
Pleasant lie almost flat, and this fact suggests that the dips flatten 
out and cause the sandstone to occur possibly within profitable reach 
of the drill. Its position, however, can be determined only by 
prospecting. 

The map (PL II) also shows that a large area on the crest and east- 
ern flanks of the Pavant Mountains is occupied by a great thickness 
of coarse conglomerate and sandstone, which are advantageously 
located to absorb water directly from precipitation and from the flow 
of streams. These coarse-textured rocks are overlain by relatively 
impervious strata and dip gently toward the valley. They are, 
however, cut by the fault which extends along the eastern base of the 
mountains, and which, by intersecting water-bearing beds, is an im- 
portant factor in connection with the water supply, as noted on page 
14. The character and position of bed rock beneath Sevier Valley 
are unknown, and the presence of this fault makes the chance of 
obtaining artesian water from this source less favorable in Sevier 

than in Sanpete Valle}^ 

«• 

WATER IN THE VALLEY DEPOSITS. 

Water absorbed at the surface percolates downward for a greater 
or less distance through the unconsolidated valley deposits until it 
reaches the zone of saturation. The upper surface of this zone is 
known as the water table, beneath which the deposits are saturated, 
the water occupying the spaces between the solid particles of gravel, 
sand, and clay. In Sanpete and Sevier valleys the position of the 
water table conforms in a general way with the contour of the valley 
floor. Beneath the broad lowlands the water table slopes at a low 
angle upstream, away from the central valley axis, but near the high- 
lands the slope of the surface of saturation is less than the inclination 
of the ground. As a result, the ground water in the lowlands lies 
close to the surface, and near the base of the mountains it lies at 
considerable depths. In the town of Mount Pleasant, for instance, 
the slope of the ground is about ITO feet to the mile, while the inclina- 
tion of the water table is about 95 feet to the mile. 

In the absence of adequate topographic maps on which the posi- 
tion of the water table could be shown by contours, the approximate 
depth to ground water is shown on Pis. V and VI by lines repre- 
senting areas in which ground water lies, respectively, at depths 
betAveen and 10, 10 and 50, and over 50 feet beneath the surface. 
This information was compiled from the well data given on pages 
51-57, which, with the location of the wells shown on the map, serve 
as an index to the available knowledge. Under much of the area in 
which the depth to ground water is shown as over 50 feet water can 



24 UNDERGROUND WATER IN VALLEYS OF UTAH. 

not be obtained within 100 feet or more, but it is impracticable to 
indicate on the map more than is shown. 

The position of the water table fluctuates measurably. It is 
highest in summer, after the period of heavy stream discharge and 
during the irrigation season, and lowest in winter, when there is 
comparatively little addition to the underground supply. A fluctua- 
tion of 20 feet has been observed in some wells, and variations be- 
tween 2 and 10 feet are common between the summer maximum and 
the winter minimum. The use of ground water tends to lower the 
water table, but in the area under consideration persistent decrease 
has not yet been marked, though in places, as in the fields below 
Manti, a loss of head has followed the sinking of many shallow wells. 
Locally in the lowlands there has been a permanent rise in the level of 
ground water, due to the return waters of irrigation, whereby former 
fertile tracts have been converted into meadow and swamp lands. 

The saturated beds contain varying amounts of water, their con- 
tent depending on the character, thickness, and extent of the deposits. 
Coarse-textured gravel and sand, by reason of their greater porosity, 
hold and transmit relatively more water than fine-textured clay, and 
the coarser deposits therefore constitute the chief underground reser- 
voirs. The wells that have been sunk in this region encounter beds 
of sand and gravel that range in thickness from a few inches to 
many feet and are separated by beds of clay of varying thickness. 
Locally these water-bearing beds have considerable horizontal ex- 
tent, and, although the details of their distribution are not known, 
experience in sinking wells has shown that beds of sand and gravel 
are of widespread occurrence, both horizontally and vertically. 

Underground water is seldom stationary, but moves very slowlj^ 
from a higher to a lower level. The velocity varies with the head 
and with the number and size of the interstitial spaces, for the move- 
ment is not in open channels, but through the minute pores between 
the solid particles of the deposits. The rate of movement is only 
a few feet a day. The highest velocity of ground water that has 
been recorded is about 100 feet in twenty-four hours, and generally 
it is much less, the ordinary rates in sand being between 2 and 50 feet 
a day. 

RECOVERY OF UlS^DERGROUND WATER. 

The total amount of underground water in Sanpete and Sevier 
valleys, if it could be computed, would be expressed in cubic miles, 
but, by reason either of its depth or through its inclusion in fine- 
lextured deposits, which do not readily yield their content, a large 
part of the subterranean store is not available. An estimate of the 
available amount is also impracticable because of the unknown extent 



^J 




5 AND SPRINGS 



i 



^ELLS AND SPRINGS 



« NorLflowiijg wellE 



I .1: 



'1^?' 




lil 







•,; .^ 






/^ 


jt: 


^^ 




/^ 


^ 


L^ 



~t^ 




MAP SHOWING APPROXIMATE DEPTH TO GROUND WATERS AND LOCATION OP WELLS AND SPRINGS 
IN SANPETE VALLEY, UTAH 



EECOVERY OF UNDERGROUND WATER. 25 

of the irregular lenses of sand and gravel which constitute the im- 
portant reservoirs. But, although figures can not be given, it is 
evident that a considerable supply of underground water awaits 
development in this area. 

RECOVERY OF WATER FROM BED ROCKS. 

Bed rocks are an important, but little developed, source of water in 
this area. A number of large springs originate in these consolidated 
deposits, and conditions for obtaining artesian wells are locally 
favorable. 

RECOVERY OF WATER FROM BED ROCK BY SPRINGS. 

Springs are a source of much water in Sanpete and Sevier valleys, 
88 being recorded on pages 58-60. These can be classed either as 
fault springs or seep springs, the water from the first class issuing 
along a fault plane, that from the second class seeping out, generally 
in low areas, where the surface intersects the ground-water table. 
Of the 88 that are listed 30 are fault springs, yielding an aggregate, 
discharge of 95 second- feet. Fault springs have their sources in bed 
rocks and commonly are located at the base of the mountains, along 
the principal planes of dislocation, prominent groups being on the 
eastern margin of Sevier Valley and on the western margin of 
Sanpete Valley, although isolated springs occur at a number of other 
places, as shown on the map. The discharge of fault springs varies 
little, if any, throughout the year; each spring commonly yields as 
much as 1 second-foot, the mean of all being over 3 second-feet, and 
one west of Fountain Green flows 12.4 second-feet. (PI. IV, A.) 

The temperatures of these springs differ greatly. That of many is 
only a few degrees above the mean annual temperature of the valleys, 
about 48°, but some are distinctly hot, Joseph Hot Springs (No. 3 in 
list on p. 58 and on PI. V) ranging from 135° to 156° F. and Monroe 
Hot Springs (No. 5) ranging from 144° to 156° F. The temperature 
of some of the hot springs is probably due to the proximity of heated 
igneous rocks. That of others, as Eichfield Spring (No. 71), which 
is 74° F., appears to be due to the internal heat of the earth, although 
the possible influence of igneous rocks must not be ignored. If the 
temperature of the Richfield Spring be due entirely to the normal 
heat of the earth, an index is thus afforded of the depth of the water 
before it rises. If an increment of 1° F. for each 50 feet be assumed 
without allowance for cooling, a depth of 1,300 feet is indicated. 

The general occurrence of fault springs, although each one differs 
from others in details, may be illustrated by the Richfield Spring. 
(See fig. 3.) Here the porous conglomerates and sandstones that out- 



26 



TJNDERGKOUND WATER IN VALLEYS OF UTAH. 



crop on the Pavant Mountains dip toward the valley and are overlain 
by the relatively impervious Wasatch bends. The mountains have 
been uplifted along the fault at their base, and the water-bearing 
beds — the conglomerate and sandstone — have been cut by the dis- 



West 




> 

Spring 




East 



Fig. 3. — Diagrammatic section at Richfield Spring. 

placement as if by a well. In consequence the water, which is under 
pressure, rises along the fault plane, the place of actual issue being- 
determined by a series of favorable conditions by which free passage 
is maintained. 

RECOVERY OF AVATER f'ROM BED ROCK BY TUNNELS. 

The practicability of tunneling into fault planes to obtain water is 
suggested by the occurrence of springs along lines of displacement, 
and a notable successful tunnel is that of the Morrison coal mine east 
of Sterling. This tunnel was begun on a dry hillside and driven 
eastAvard toward the fault, which has not yet been reached. Water 
was encountered which in August, 1905, was found to discharge 5.6 
second-feet. The probable conditions here are shown by fig. 4. The 
source appears to be in the westward-dipping sandstone that outcrops 
on the Wasatch Plateau. The water being under hydrostatic pres- 




FiG. 4. — Diagrammatic section at Morrison Tunnel Spring. 

sure, rises when it reaches the fault plane. Notwithstanding the 
success of this tunnel, similar results can not be generalh^ predicted, 
because of the ever-present possibility of unfortunate conditions, 
such as cementation along fault planes and easier escape of the water 
in other directions. Yet tunneling into fault planes along which 
strong springs occur presents possibilities that would seem to justify 
prospecting. 

Tunnels may be advantageously driven not only into fault planes, 
but possibly elsewhere, for it may be profitable to explore locally the 



RECOVERY OP UNDERGROUND WATER. 27 

base of the mountains where water-bearing beds dip valleyward, as 
in the Pavant Range and on the Wasatch Plateau, with the idea of 
penetrating saturated strata by tunnels instead of wells. 

RECOVERY OF WATER FROM BED ROCK BY WELLS. 

With the exception of well No. 237 (see list on p. 56, and map 
forming PL VI), between Mount Pleasant and Fairview, no wells, as 
far as the writer is informed, have been sunk to bed rock in Sanpete 
and Sevier valleys. Nevertheless flowing wells may possibly be 
obtained from consolidated rocks in certain areas as already sug- 
gested, the most promising sources being the eastward-dipping con- 
glomerates and sandstones on the Pavant Mountains and the west- 
ward-dipping sandstone on the Wasatch Plateau. 

Steep dips and faults are locally disturbing factors, but the con- 
ditions warrant sinking test wells. 

In the centet- of Sevier Valley, on account of the faulting, it is pos- 
sible that the water-bearing beds lie at depths too great for profit- 
able wells, since the temperature of the Richfield Spring indicates 
a depth of 1,300 feet to the water beds at the border of the valley. 
Preliminary tests might be made west of the fault in valleys where 
streams have cut deep into the rocks. 

Conditions for flowing wells are more favorable in Sanpete Valley, 
especially between Fairview and Spring City. The absence of fault- 
ing has not been proved here, but the westward-dipping rocks of the 
Wasatch Plateau may extend unbroken beneath the valley, where the 
dips probably flatten out. If these conditions actually prevail it is 
likely that profitable flowing wells can be obtained from the Laramie 
sandstone. Because of the uncertainty of the dip and the variable 
thickness and unknown erosion of the Eocene strata depths can not 
be predicted, but before a test well is abandoned it should be sunk 
until the Laramie sandstone is reached. 

RECOVERY OF WATER FROM VALLEY DEPOSITS. 

The source of most abundant underground water in Sanpete and 
Sevier valleys is the unconsolidated material by which they are 
underlain and from which water is recovered by springs, tunnels, 
and both flowing and nonflowing wells. 

RECOVERY OF WATER FROM VALLEY DEPOSITS BY SPRINGS. 

Although most of the fault springs issue through unconsolidated 
deposits, their origin is obvious and they should not be confounded 
with seep springs. As already stated, springs of the first class occur 
along faults. Those of the second are independent of structure and 
commonly occur in lowlands where the surface of the ground inter- 



28 



tTNDEEGROUND WATER IN VALLEYS OF UTAH. 



sects the water table. The discharge of seep springs is generally 
unlike that of fault springs, since it often fluctuates with the season 
instead of flowing almost constantly. The temperature of fault 
springs is also more constant, and is commonly higher than that of 
seep springs, a fact that is especially apparent during the winter. 

Seep springs are numerous in Sanpete and Sevier valleys, espe- 
cially in their lower stretches, and the important part played by 
seepage in maintaining the flow of the streams has been already noted. 
Seepage is so widespread and in any one spot is usually so slight that 
over large areas it is impracticable to map places of exit of seepage 
water, but points where the flow appears in springs and is concen- 
trated into considerable streams are shown on Pis. V and YI and 
are listed on pages 58 to 60. The flow of many seep springs can be 
increased by development, but some of them are at elevations so low 
that their waters are unavailable for use in the immediate vicinity 
except by pumping. 

RECOVERY OF WATER FROM VALLEY DEPOSITS BY TUNNELS. 

Tunnels driven into the unconsolidated deposits have procured 
large amounts of water. Especially favorable sites for tunnels are 
places where the low lands begin to raise at an increased angle toward 
the base of the mountains. At such places the ground water tapped 




Fig 5 —Section illustrating a tunnel m the valley deposits 

will drain by gravity into tunnels, as illustrated in fig. 5. A tun- 
nel of this class is that of Madsen and Seely, west of Mount Pleasant. 
(See p. 49.) 



RECOVERY OF WATER FROM VALLEY DEPOSITS BY NONFLOWING WELLS. 

Nonflowing wells, the general features of which are indicated in 
the list, pages 51-57, are the most common means of recovering under- 
ground water in Sanpete and Sevier valleys. The maps show that 
ground water lies within 10 feet of the surface under a large part of 
the valleys, this area of course being in the lowlands, and that toward 
the highlands the depth increases. The nonflowing wells are com- 
monly dug beneath the ground-water level to a porous bed of sand 
or gravel, from which water percolates into the opening. Most of 



RECOVERY OF UNDERGROUND WATER. 29 

the wells are sunk several feet below the summer stage of the water 
table in order to provide for the seasonal fluctuation. There are also 
a number of nonflowing bored wells, which have been put down with 
the hope of obtaining a flow at the surface. 

Water is drawn from most of these wells by buckets or hand 
pumps. A few windmills are in operation, but the wind velocity is 
apparently not great or steady enough to give them general favor. 
There are few, if any, power pumps in the valley, which affords a 
promising field for their introduction and their use in irrigation. 
Water contained in coarse beds, which insure an abundant yield, lies 
within easy reach of the surface beneath large areas, and electric 
power can be cheaply developed from the near-by mountain streams. 

RECOVERY OF WATER FROM VALLEY DEPOSITS BY FLOWING WELLS. 

The irregular sheets of gravel, sand, and clay that slope valley- 
ward from the base of the mountains afford conditions favorable 
for j)ressure in their contained water. Accordingly, where beds of 
sand and gravel that lie below a confining stratum of relatively im- 
pervious material are encountered by wells which enter the zone of 
saturation, the water tends to rise in the wells, and in the lowlands 
sufficient head is developed to cause flows at the surface. Above the 
lowlands on each side of the valley the water in deep wells rises a 
greater or less distance, the height it reaches depending upon the 
elevation of the ground. 

It is estimated that there are more than 100 flow^ing wells in the 
tw^o valleys, yielding an aggregate flow of about 5 second-feet. Most 
of the wells are 1^ or 2 inches in diameter, but a few of the larger 
ones are 3 or 4 inches. Flows are obtained at different depths be- 
tween 20 and 344 feet, under pressures at the surface varying from 
to 6 pounds per square inch. The average yield of the wells is 
possibly about 20 gallons a minute, but the range is wide, several 
discharging less than 1 gallon a minute. The greatest flow^ measured 
was 160 gallons a minute, from a 3-inch pipe. Beneath the first flow 
other flows are commonly obtained from each bed of sand and gravel 
encountered in boring the well. 

The flow^ing wells are located in the fields below the towns, which 
generally are built at elevations so high that the water of the wells 
is little used for domestic purposes, for which, by its purity, it is 
eminently adapted. It is used to some extent for watering stock, 
but chiefly for irrigation. 

The use of artesian water from the valley deposits has only begun, 
and the possibilities apparently are not realized. There is need for 
a number of test wells to exploit conditions in the lower deposits, 
and where good flows are obtained more wells of larger bore may 
profitably be sunk. 



30 



UNDEEGKOUND WATEE IN VALLEYS OF UTAH. 



RECOVERY OF WATER FROM VALLEY DEPOSITS BY SUBSURFACE DAMS, ETC. 

Under exceptional conditions ground water may be recovered 
by means of subsurface dams or similar contrivances which impound 
the underflow in unconsolidated materials. These conditions are prac- 
tically impervious bottom within easy reach of the surface, to pre- 
vent excessive lowering of the ground-water level, and competent 
side walls, not too far apart, to intercept lateral escape. The 
presence of these conditions can be determined only by prospecting, 
and the economic desirability of building such structures at par- 
ticular places is an independent question, but because of the high 
value of water in this area their feasibility at each possible site 
should be investigated. Possible locations of subsurface- dams are 
suggested by rock walls at the mouths of the narrow canyons, where 
borings in search of suitable bottom should be made. Tests of the 
amount and porosity of the valley filling at and above the mouths 
of the canyons, together with measurements of the velocity of the 
underflow, would indicate the quantity of ground water available. 
At some places below the mouths of the canyons in the several creek 
valleys conditions favorable to the construction of infiltration gal- 
leries may also be discovered. 

QUALITY OF WATER. 

Few analyses have been made of the waters of Sanpete and Sevier 
valleys, although their general character is indicated by a number 
of field tests. During the summer of 1900 the Bureau of Soils « 
examined the waters of Sevier Valley, and in the fall of 1905 the 
writer made the following field assays, using the methods suggested 
by Mr. M. O. Leighton.^ The figures given represent only approxi- 
mate composition ; yet, as all the tests were made under similar con- 
ditions, they afford rough comparative data : 

Field assays of water from Sanpete and Sevier valleys, Utah. 

[Parts per millon.] 



Name and locality. 



STREAMS. 

Pleasant Creek c 

MantiCreekc 238 204 157 Trace. 

San Pitch Creek, west of Mount Pleasant 890 408 237 45 

San Pitch Creek, east of Gunnison 550 408 492 519 

Sevier River, west of Gunnison 1,150 377 +626 1,015 

Sevier River, west of Joseph 261 80 29 

Sixmile Creek c 360 245 65 19 

Twelvemile Creek c 505 76 19 

Upper Salina Creek, 7 miles above mouth of canyon. 410 245 113 9 

« Soil survey in Sevier Valley, Utah, Rept. field operations Division of Soils, U. S. Dept. 
of Agriculture, 1900. 

» Leighton, M. O., Field assay of water : Water-Sup. and Irr. Paper U. S. Geol. Survey 
No. 151, 1905. 

c Samples obtained at mouths of canyons. 



Calcium 

(Ca). 


Bicarbon- 
ate radicle 


Sulphate 
radicle 


(HCO3). 


(SO4). 


238 


234 


- 35 


238 


204 


157 


890 


408 


237 


550 


408 


492 


1,150 


377 


+626 


261 




80 


360 


245 


65 


505 




76 


410 


245 


113 



Chlorine 

(CI). 



QUALITY OF WATER. 



31 



Field assays of icater from Sanpete and Sevier valleys, Utah — Continued. 



Name and locality. 



STREAMS — continued. 



Lower Salina Creek a 

Monroe Creek « 

Dry Creek a 



Fountain Green (No. 86)& 
Morrison tunnel (No. 38) . 
Ninemile (No. 34) 



Glenwood (No. 12). 
Richfield (No. 16).. 



FLOWING WELLS. 



Allred 

Seeley 

West of Manti , 

Between Fairview and Mount Pleasant , 

Bolitho 

Brooklyn Irrigation Co , 



DUG WELLS. 



Fairview (Boliney House) . . 

Salina (White House) 

South of Salina (Colby) 

Ephraim (S. Sorensen) 

Moroni (Moroni House) 

Ephraim (Ephraim House) . 
Gunnison (Gunnison House) 



Calcium 

(Ca). 


Bicarbon- 
ate radicle 


Sulphate 
radicle 


(HCOa). 


{SO4) 


151 


265 


127 


96 


102 


- 35 


248 




53 


(«) 


265 





410 


326 


164 


435 


367 


459 


96 


122 





228 


265 


Trace. 


380 


408 


492 


274 


204 


- 35 


274 


367 


135 


274 


286 


- 35 


340 


326 


74 


595 


326 


530 


715 


367 


- 35 


595 


510 


135 


320 


204 


108 


1,150 


551 


+626 


650 


367 


300 


274 


449 


62 


248 


571 


572 



Chlorine 

(CI). 



119 
9 



297 

258 

14 

19 

59 



19 

218 
109 
148 
258 
59 
636 



« Samples obtained at mouths of canyons. 
" Numbers are those given on Pis. V and VI. 
<^ Calcium content very large. 

The general composition of the waters of the area under considera- 
tion can be inferred from the outline of the gealogy of the watershed, 
for the mineral content of surface and ground waters is determined 
by the chemical character of the rocks and soils with which they come 
in contact. (See pp. 8-14.) The prevalence of limestone causes an 
abundance of carbonates ; the waters which come under the influence 
of the Jurassic salt and gypsum bearing rocks are rich in chlorides 
and sulphates; while streams like Monroe Creek, which traverse 
igneous rocks, carry relatively little mineral matter in solution. 
Water from wells of moderate or considerable depth is usually 
similar to that of the mountain streams in the same locality, but 
that from shallow wells in the lowlands, especially in irrigated tracts, 
Contains abundant dissolved salts. This mineral content is largely 
derived from the return waters of irrigation, which leach the soils, 
for in the lowlands where ground water is within reach of capillary 
action the dissolved salts are deposited by evaporation and the soil 
is impregnated w^ith an accumulation of " alkali." The combined 
deleterious effects of the soluble Jurassic rocks and of the alkali in 
the lowlands is shown in the table by the two tests of the water of 
Sevier Kiver. The sample collected Avest of Joseph, in the upper 
part of the valley, contained only 261 parts per million of calcium, 
80 sulphates, and 29 parts of chlorines, while the sample from the 



32 UNDERGROUND WATER IN VALLEYS OF UTAH. 

same river west of Gunnison contained 377 parts of bicarbonates, 
1,150 parts of calcium, over 626 parts of sulphates, and 1,015 parts 
of chlorine. 

The natural conditions are generally favorable for obtaining good 
water for domestic purposes, but the communities give little heed 
to the sanitary character of the water, and as a result epidemics of 
typhoid fever of greater or less violence are not uncommon. As ordi- 
nary hygienic precaution will prevent most of such epidemics the 
negligence in providing pure water supplies can not be too strongly 
condemned. Ill-kept privies and cesspools are nuisances that should 
not be tolerated in settled communities. Privies should be replaced 
by " dry-earth closets," provided with a supply of dry clay loam, 
and the fecal matter should be removed at short intervals. Where 
there are public water supplies it is desirable that sewers should also 
be installed and the sewage might, if desired, be used in irrigation 
on " sewer farms." The local custom of using old wells as cesspools 
pollutes the water of neighboring wells that are still used as sources 
of drinking water, and should be prohibited. Another prevalent 
unsanitary custom is the use, for drinking and cooking, of water 
running through the towns in open ditches, into which pollution 
is free to drain. 

All the towns in the area except one or two can procure water sup- 
plies either from springs or from mountain streams, which with care 
can be protected from contamination, and outlying houses can be sup- 
plied with water from deep wells. But although pure water can 
easily be obtained, only four towns in Sanpete and Sevier valleys^ 
Freedom^ Mount Pleasant, Manti, and Richfield — have public water- 
works. 

SUGGESTIONS. 

In view of the present undeveloped state of the ground waters of 
Sanpete and Sevier valleys and the need of more water, a few sug- 
gestions as to a more efficient use of the available resources may be 
pertinent. 

As the only source of water is the precipitation on the drainage 
area tributary to the valleys, it is clear that attention should be given 
to conserving this supply by preventing waste whenever possible. 
The chief problem is to save the storm waters, and to this end large 
storage reservoirs have been built or planned, but it does not appear 
to be generally realized that the storm run-off can be saved also by 
other means. The underground supply can be considerably aug- 
mented by distributing the flood discharge over the uplands below 
the mouths of the canyons of the creeks that emerge from the moun- 
tains. The control of floods is difficult, but by placing obstructions 
in the ordinary channels flood waters can be spread over a wide area, 
so as to increase greatly the amount of water that is absorbed in the 



SUGGESTIONS. 33 

porous alluvial deposits. Small reservoirs can also be constructed at 
many places within the mountain watershed, whereby the storm run- 
off can be checked and the seepage run-off in the dry season increased. 
The advantage of preserving timber on the mountains should also be 
clearly understood. A drainage area well covered with vegetation 
is one of the most effectual checks to storm run-off. A heavy growth 
of underbrush and trees tends to prevent storms from washing away 
the products of rock decay and to accumulate a thick cover of soil 
and humus, which absorbs large quantities of water from storms and 
from melting snow, whereas if the covering of vegetation is scant, 
storms tend to keep the mountain sides relatively bare of soil by 
washing the debris into the creeks, so that the precipitation runs off 
rapidly and comparatively little is absorbed to seep slowly into the 
creeks to maintain their summer flow. The timber should therefore 
be protected from fire and from reckless cutting, excessive grazing 
should not be permitted, and trees might be planted to advantage in 
many areas. 

Not only should the supply be conserved as far as possible, but 
more efficient use of the available water should be practiced. Much 
is lost by crude methods of irrigation. More water is often applied 
to the fields than is needed, and a large part is lost by seepage from 
faultily constructed ditches. The use of pipes whenever practicable 
and the construction of less permeable canals would prevent much 
waste. Much water is also lost by allowing artesian wells to flow con- 
stantly. It should be thoroughly realized that the limited supply 
of ground water comes from a common source, that the wastefulness 
of one person counteracts the prudence of another, and that the in- 
terest of all demands that the supply be rigorously conserved. Flow- 
ing Avells should be capped, or the flow should at least be partly 
checked when water is not used, or the water should be collected in 
reservoirs for future use. A further incentive to economy in the use 
of water is the fact that by its conservation the evil of alkali accumu- 
lation and the raising of the water table too near the surface in the 
lowlands is retarded. 

The distribution of underground water suggests that the most effi- 
cient use of the total supply in the valley would be to develop the 
fertile uplands toward the base of the mountains, as far as may 
be, from high-line canals, supplied by the mountain streams; and 
to use underground water, which in general is inaccessible on the 
uplands, in developing the lowlands, where the subterranean supply 
is plentiful. Owning to the present complicated ownership of water 
rights, it may be difficult to act upon this suggestion, but there can be 
no doubt that its adoption would materially add to the amount of 
land under cultivation. Flowing wells can be obtained in large areas 

IRB 199—07 M 3 



34 UNDEHGEOUISrD WATEE IX VALLEYS OF UTAH. 

in the lowlands, and at several localities where coarse water-bearing 
sand and gravel occur near the surface there is a possibility of estab- 
lishing pumping plants, for which electric power developed from the 
adjacent mountain streams is generally available. It should be 
remembered, however, that although the underground supply is con- 
siderable, it must not be recklessly used. Observations on the fluc- 
tuation of the water table should serve as a guide to development. 

Since the underground water supply in Sanpete and Sevier valleys 
is but little developed and local conditions are promising, further 
testing of the resources is very desirable. Deep wells should be 
sunk in both valleys to ascertain the conditions in the unconsoli- 
dated deposits, and to determine whether flowing wells can be ob- 
tained from bed rock. Where good supplies are found pipes of 
larger bore than those now used might well be employed. Also the 
flow of some of the springs can be materially increased by develop- 
ment, and possibly new ones found by prospecting. 

DETAII.ED DESCRlPTIOlSrS. 

The descriptive details that follow are supplementary to the infor- 
mation contained in the maps forming Pis. YI and VII and the list 
of wells and springs on pages 51-60. The descriptions begin at the 
south and proceed northward, the areas described being grouped 
about the principal towns. 

JOSEPH AND VICINITY. 

About 6 miles south of Joseph the Sevier Kiver emerges from a 
canyon aaird flows northeastward between the lava-capped foothills 
of the Pavant Mountains and a low ridge of igneous rocks. The 
town of Joseph is situated near the base of the long alluvial slope 
west of the river. Water for irrigation is furnished by the Sevier 
Valley canal, below which most of the land is under cultivation, and 
drinking water of poor quality is obtained from shallow dug wells. 
Most of the area lying below the canal is underlain by gravel and 
by subordinate streaks of sand and clay; ground water lies within 
50 feet of the surface, and the wells are between 30 and 60 feet in 
depth. The annual fluctuation of the water surface amounts to 
about 10 feet, the water being highest in midsummer and lowest in 
late winter, when some of the wells go dry. A better supply for 
drinking purposes probably can be obtained from bored wells near 
the river, 100 feet or more in depth. These would avoid contamina- 
tion and at least some seepage from the canals. There is little likeli- 
hood of profitably obtaining underground water for irrigating the 
arid slope west of Joseph, although it is possible that deep wells, 
after penetrating a considerable but unknown thickness of lava and 



DETAILED DESCRIPTIONS. 35 

the underlying Eocene strata, would strike artesian water in the 
underlying sandstones and conglomerates. 

The Joseph Hot Springs issue from calcareous tufa, deposited by 
the springs, at the base of the low volcanic ridge about a mile south- 
east of the town. The temperature of the water ranges from 135° 
to 146° F., and the yield of all is estimated to be only about 30 gallons 
a minute. 

ELSINORE AND VICINITY. 

Sevier Valley broadens out a few miles above Elsinore, which is 
located in the midst of a prosperous agricultural district. Contigu- 
ous to the river, particularly south of it, a number of shallow wells 
have been dug, from which an abundant supply of water in coarse 
gravel is obtained at depths ranging from 20 to 35 feet. Two wells 
have been bored in this area, one, 178 feet deep, in the SE. J sec. 32, 
T. 24 S., E. 3 W., the other, 171 feet deep, in the SW. i sec. 34, in 
the same range and township. In sinking these wells the surface 
was found to be underlain chiefly by sand and gravel to a depth of 
150 feet, where stiff yellow clay was encountered, through which the 
inadequate apparatus failed to penetrate. This immediate area is 
favorable for testing underground conditions, and it is desirable 
that a deep well be sunk here to determine the possibility of obtain- 
ing flowing wells in the valley deposits. The discharge of Monroe 
Creek, on the southeast, and the seepage from Sevier River in its 
sandy course below the mouth of its canyon are sources of an under- 
ground supply which may be under pressure in ]DOSsible coarse de- 
posits beneath the clay above mentioned. If flowing wells should 
not be obtained, pumping from the shallow gravels is an attractive 
possibility. 

Midway between Joseph and Elsinore, near the river, in SE. J 
sec. 6, T. 25 S., R. 3 W., there is a group of about 25 wells, in w^hich 
the water rises within 2 or 3 feet of the surface. These are IJ inches 
in diameter and less than 50 feet deep and the yield of all amounts 
to about 1 second-foot. Trenches have been dug, in which the flow is 
conducted to the Brooklyn canal. Clay was encountered in these 
wells down to 12 feet, below which water-bearing sand and gravel 
occur. 

The town of Elsinore is built on an alluvial slope at the base of 
lava-capped foothills. Water for irrigation is obtained from several 
canals that are fed by Sevier River, and these also furnish an unsat- 
isfactory domestic supply, which is supplemented by a few poor 
wells between 60 and 115 feet in depth. The chief desideratum is a 
good supply for domestic purposes. Possible sources are a number 
of feeble seep springs in the hills a few miles to the northwest, 
springs on the east side of the valley adjacent to Thompsons Creek, 



36 UJSTDEEGROUND WATER IN VALLEYS OF UTAH. 

Monroe Creek, and wells. Although capable of development, the 
yield of the springs first mentioned appears to be insufficient ; on the 
other hand, surface water of good quality and abundant quantity is 
available on the eastern side of the valley, but its use necessitates a 
pipe line extending several miles. The project of sinking wells, 
however, offers attractive possibilities. These are of two distinct 
classes, deep wells in the valley deposits and wells sunk to bed rock. 
The desirability of sinking a test well in the valley south of Elsinore 
has just been mentioned. It can hardly be expected, even if a flow 
should result, that the pressure would be sufficient to carry the water 
to Elsinore, yet it is probable that water of good quality can be thus 
obtained. Another possibility is to tap the sandstones and con- 
glomerates that cap the Pavant Mountains and dip southeastward. 
The fault along the base of the mountains complicates the situation 
and makes it desirable that the first experimental well be drilled west 
of it. Another disturbing factor in the vicinity of Elsinore is the 
cap of hard lava. This, however, can be avoided by sinking a well 
in the valley about 2 miles north of the town. The surface strata 
will probably yield water of poor quality, but this could be cased off, 
for good water under pressure is to be expected from the underlying 
beds. The depth at which water will be found can not be predicted, 
but the beds that overlie the water-bearing strata are probably several 
hundred feet thick, and if exploration is undertaken at all prepara- 
tions should be made to sink a well at least 1,000 feet deep. 

MONROE AND VICINITY. 

Monroe is prettily situated on an alluvial slope on the east side of 
the valley, at the base of the Sevier Plateau. Monroe Creek, the 
principal source of water supply, flows throughout its course over 
cystalline rocks, and its water therefore contains relatively little dis- 
solved matter. In this respect it is the purest large stream in the 
entire area here considered. A number of canals, fed from Sevier 
Eiver and Monroe Creek, furnish water for irrigation, and these 
canals are also largely resorted to for domestic supply. In view of 
the fact that excellent water is available in Monroe Canyon, it is 
surprising that the community is willing to continue using for house- 
hold purposes the present relatively unsanitary supply. The depth 
to ground water is over 50 feet, and there are but few wells in 
Monroe. 

The hot springs near Monroe are a valuable asset, but as yet they 
are little used. There are several groups of springs a half mile east 
of the town along a probable fault line at the base of the mountains, 
which are composed of igneous rocks. The salts held in solution by 
the water are deposited as tufa, from which springs now issue at a 
Iiumber of places. The total yield is about 100 gallons a minute^ and 



DETAILED DESCRIPTIONS. 61 

the temperature of the water when it reaches the surface ranges from 
144° to 156° F. The proximity of the springs to the town suggests 
the desirability of attempting to increase their flow with the idea of 
utilizing the leat. 

The following analysis of the water of Cooper Hot Springs was 
obtained from the owner: 

Analysis of umter from Cooper Hot Springs, east of Monroe (No. 5). 

[Analyst, P. A. Yoder.] 

Parts per million. 

Ca 267. 7 

Mg 35. 1 

Na 591.4 

K 37. 5 

Li .6 

Fe, Al 0.0 

SiO, 23. 5 

SO, - 167.6 

CO3 - 36.0 

CI 684.6 

Total solids 1,794.0 

The few Avells that have been sunk in the valley southwest of Mon- 
roe show that the depth to ground water is over 70 feet. The most 
practicable way, therefore, of developing the area is from high-line 
canals supplied by Sevier River and Monroe Creek. 

The presence of several springs between 1 and 3 miles south of the 
mouth of Monroe Canyon, along a probable fault, suggests that 
more water may be obtained by tunneling. 

RICHFIELD AND VICINITY. 

The portion of Sevier Valley between Monroe and Richfield that 
lies below the canals is in large part under cultivation, but the por- 
tion above them consists of desert alluvial slopes that extend up to 
the bases of the mountains. In the highlands bowlders and coarse- 
textured debris abound, while the lowlands are floored with sand and 
clay loam. The map forming PI. VI shows that ground water 
lies within 10 feet of the surface under a considerable part of the low- 
lands, and that in this vicinity there are about 100 artesian wells, 
concerning which representative data are given in the list on pages 
51-57. They are shallow, ranging from 50 to 95 feet in depth, and 
yield from 3 to 142 gallons a minute under a pressure at the surface 
of slightly over 2 pounds. In drilling, clay is usually encountered 
for 40 to 60 feet, below which lies said and gravel, Avhence the flows 
are obtained. The gravel appears to be widely distributed and con- 
stitutes a valuable reservoir. By a single well, No. 59, in list on page 
52 and map (PL V), which is 4 inches in diameter, 62 feet deep, 



38 UNDERGROUND WATER IN VALLEYS OF UTAH. 

and yields 132 gallons a minute, a large tract of alkali land has been 
converted into an excellent meadow. 

The deepest well in this vicinity was sunk in 1900 in NE. ^ sec. 7, 
T. 24, S., R., 2 W., to a depth of 324 feet. The log of this well, as re-, 
ported by the owner, is given below : 

Log of well in sec. 7, T. 21, S., R. 2 W., in feet. 



Clay 

Sand and gravel 

Clay 

Sand and gravel 
Clay 

Sand and gravel 



Thick- 



Depth. 



62 


62 


88 


• 150 


15 


165 


B5 


300 


20 


320 


24 


324 



From the upper beds of sand and gravel in this well water rose 
within a few inches of the surface and a flow was obtained from the 
bottom, but the pipe broke and the well was discontinued. So far as 
known, this is the deepest hole in Sevier Valley proper, and the re- 
sults serve to emphasize the desirability of a deep test well. The 
probabilities are that such a well will penetrate one or more beds of 
sand and gravel, bearing water under pressure great enough to cause 
flows at the surface, even if the well should be sunk at some distance 
from the river. 

Not only the valley deposits, but the bed rock is an available 
source of underground water, especially along the base of the moun- 
tains, near Richfield. The considerable outcrop of sandstone and 
conglomerate on the crest and eastern flanks of the Pavant Range, 
as already stated (p. 23), presents a large area for the absorption of 
precipitation and run-off, and the eastward dip and cap of Eocene 
strata cause the contained water to be under pressure. Although 
deep valleys drain a large portion of the porous rocks, it is neverthe- 
less likely that a well sunk through the capping of limestones and 
shales will strike artesian water in the underlying sandstone and 
conglomerate. The fault along the base of the mountains is a dis- 
turbing factor, yet apparently it is the cause of the spring west of 
Richfield, and thus serves to emphasize the possibility of obtaining 
water under pressure. The depth at which water may be expected 
can not be closely predicated. If a test well is attempted provision 
should be made for driving 1,000 feet or more, the depth depending 
on the location of the well; the farther away from the mountains 
it may be dug the deeper it will need to be sunk to reach the water- 
bearing beds. A rough approximation of the depth to the Richfield 
spring water may be afforded by its temperature, 74° F., which is 
26° above the mean annual temperature. If the temperature be due 
to the internal heat of the earth, which, it is assumed, increases about 



DETAILED DESCKIPTIONS. 39 

1 degree in every 50 feet, the water is derived from a depth of about 
1,300 feet. It is possible, however, that the water owes its tempera- 
ture in part to the proximity of heated igneous rocks. 

Inverury and Annabelle, small towns situated on opposite sides of 
the Sevier, 4 miles south of Richfield, are supported by irrigation 
from canals fed by the river. Inverury is supplied w^ith poor drink- 
ing water from shallow wells, although water of better quality can be 
obtained by driving deeper and casing off the upper flow. Anna- 
belle, on the other hand, derives a good supply for domestic use from 
reservoirs in the mountains south of the town. 

Richfield, the commercial center of Sevier Valley, has a population 
of about 2,000. The town is situated at the foot slope of the Pavant 
Range, and derives its water supply from the Sevier Valley and 
other canals and from the spring referred to on page 25. This 
spring, discharging 3.2 second-feet, besides furnishing water for local 
irrigation, supplies the city waterworl^ — the best system in the 
entire area considered in this report. The spring is inclosed in a 
brick structure, whence the water is piped to a concrete reservoir 
and distributed through an 8-inch main. Before the waterworks 
were installed the town depended largely upon wells that range in 
depth from 15 to 20 feet. Some of these are still used ; others have 
been abandoned and are used as cesspools, thus introducing a source 
of contamination which should not be tolerated. 

Glenwood is prettily located in a cove, at the base of Sevier Plateau, 
that is separated on the west from the main valley by a low lava- 
capped ridge. The tow^n and its vicinity are supplied with water for 
irrigation and domestic use by springs. . East and west of the lava- 
capped ridge there are springs whose discharge aggregates about 20 
second-feet. Those on the west side of the ridge are reported to have 
broken out since 1880, and their flow is so copious that a considerable 
area has been converted into marsh land. The conditions here can be 
improved by drainage and by conveying the surplus water where it 
is more needed. The springs on the east side of the ridge discharge 
9 second -feet and are the source of Cove Creek. At an elevation of 
250 feet above the town Glenwood Springs issue from debris at the 
base of igneous hills and form the main local supply for all purposes, 
the discharge being 7 second-feet. Although the supply is plentiful, 
a needed improvement is the installation of a waterworks system that 
would do aw^ay wdth the present insanitary practice of obtaining 
domestic water directly from open ditches in the streets. The springs 
also afford an excellent source of power, which is as yet undeveloped. 
North of Glenwood, along the base of the mountains, there are other 
springs, notably Herrins Hole Springs and Black Knoll Springs, 
which yield respectively 1 and 12 second- feet. All of these springs 
probably rise along faults. 



40 UNDEBGKOUKD WATER IN VALLEYS OF UTAH. 

SALINA AND VICINITY. 

Between Richfield and Salina the character of the country changes. 
On the east of the valley the Sevier Plateau, an area of igneous rocks, 
slopes rapidly northward to the interval separating it from the Wa- 
satch PJateau, which is underlain by sedimentary rocks. A narrow 
belt of gypsiferous drab and red shales, capped here and there with 
lava, lies between the base of the plateaus and Sevier River. On the 
west side of the valley the eastward-dipping Eocene beds of the Val- 
ley Mountains are separated by a fault from the red conglomerates 
and sandstones of the Pavant Range. The appearance of the valley 
also changes. West of the river the canals water a relatively narrow 
strip, beyond which there is a long desert slope up to the base of the 
mountains, while on the east still less land is irrigated from small 
ditches fed by creeks. 

I Here, as throughout the valle}'^, the lowlands are superficially under- 
lain by fine-textured soils, while the foot slopes of the mountains are 
littered with coarse debris. Ground water lies between 10 and 50 feet 
from the surface in a belt contiguous to the river, where most of the 
wells have been sunk. They are chiefly driven wells, 2 or 3 inches in 
diameter and from 100 to a little over 200 feet in depth. This depth, 
unusual in Sevier Valley, is necessitated by the strongly saline 
character of the water nearer the surface, due to the proximity of the 
salt and gypsum-bearing shales. The wells first penetrate about 60 
feet of clay, below which lie alternating layers of gro^vel and clay. 
Each gravel bed yields water under pressure that causes it to rise 
within a few feet of the surface. Along the entire length of Sevier 
Valley, between Venice and Gunnison, the character of the ground 
water is impaired by salts leached from the adjacent Jurassic beds. 
These salts, however, apparently do not permeate the valley deposits 
throughout their entire thickness, but seem to be confined largely to 
the upper layers by beds of clay, so that water of better quality is 
obtained by deep wells. 

I The character and structure of the bed rocks in the highlands im- 
mediately adjacent to the valley between Richfield and Salina are not 
in general favorable for storing or yielding much water, but water 
under pressure probably can be obtained in the red sandstone and con- 
glomerate north of Richfield (p. 10). Artesian water ma}^ prob- 
ably also be obtained in the valley of Salina Creek, several miles 
above Salina, a probability which, in view of the needs of the town, 
becomes important. As has been stated in the outline of the geology 
of the region (p. 9), thick sandstones that dip westward at a Ioav 
angle and are overlain by Eocene beds outcrop in the upper valley of 
Salina Creek. Here the opportunities for absorption are good, and 
it is likely that wells that penetrate to saturated horizons of the sand- 



DETAILED DESCRIPTIONS. 41 

stone will strike artesian water. If a test well be sunk it should be 
located at least 5 miles up the creek from Salina, for a fault probably 
lies between the small outcrop of Colorado age and the water-bearing 
beds. 

Salina is situated at the base of the salt and gypsum bearing shales, 
near the mouth of Salina Creek. The town obtains its supply of 
water for domestic uses from ditches fed by the creek, and from dug 
wells, but the water from both sources is of poor quality. An effort 
was made in 1905 to obtain good water by sinking a 4-inch well to 
a depth of 163 feet, where water was encountered which rose within 
42 feet of the surface. The site was not particularly good and the 
depth not great, so the test proved unsuccessful. 

Log of Salina town tvell, in feet. 



Clay and sandy soil. 

Sand and gravel 

Hard white layer. . . 
Sand and gravel 



Thick- 



Depth. 



35 


35 


91 


126 


24 


150 


13 


163 



A sample of water from the lower sand and gravel in this well was 
analyzed by H. Harms, of Salt Lake City, and found to contain 1,708 
parts per million of dissolved solids, 728 of which are chlorine. 
This large content of salts renders the water undesirable for drink- 
ing purposes. A number of families have their drinking water 
hauled from Colby's well (No. 85 on map), about 4 miles southwest 
of Salina, which is reported to contain only 576 parts per million of 
dissolved salts, but this practice is only a makeshift. Further tests 
should be made with deep wells in the valley, away from the imme- 
diate influence of Salina Creek, and deep enough to escape seepage of 
Avater containing salts derived from the adjacent hills. It is desira- 
ble also that a test be made for artesian water up the valley of Salina 
Creek. The nearest good surface water is derived from feeble streams 
in the Pavant Mountains and from Salina Creek above the belt of 
saline rocks. 

The small town of Aurora, 5 miles southwest of Salina, is supplied 
mainly by canals. A few wells, over 100 feet in depth, here obtain 
a fairly good supply beneath the saline surface water. The water 
rises in these wells within 20 or 40 feet of the surface. It is desira- 
ble that a deep test well be sunk in this part of the valley to determine 
whether water of good quality can be obtained under pressure suffi- 
cient to flow at the surface. It is possible that the spring 2 miles 
w^est of town can be developed so as to yield enough water for do- 
mestic uses. 



42 UNDERGROUND WATER IN VALLEYS OF UTAH. 

Redmond is plentifully supplied with water, its chief asset being 
the springs that feed Redmond Lake. These issue from the bottom 
and edges of the lake and discharge about 13.5 second- feet. The 
temperature of one small spring of the group in August, 1905, was 
70° F., which, together with the large amount of water the springs 
yield, suggests that they occur along a fault, which, however, has 
not been traced on the surface. Ditch water is generally used for 
domestic use, and little attention is given to its sanitary character. 
By fencing the lake and piping the supply used for drinking, water 
of excellent quality can be cheaply obtained. Ground water occurs 
within 10 feet of the surface in the lower part of the town, although 
there are but few wells. One well (No. 106 on the map), about a 
mile northeast of Redmond, was sunk to a depth of 180 feet passing 
through the following material : 

Log of tvell No. 106, in feet. 



Thick- 



Depth. 



Clay 

Sand and clay 

Clay 

Gravel 

Clay 



20 

- 103 

120 

142 

180 



Water in the lower gravel rises within 3.5 feet of the surface. 

GUNNISON AND VICINITY. 

A few miles north of Redmond, west of the river, there is a narrow 
belt of low hills, below which the valley broadens, reaching a width 
of 9 miles at Gunnison. The lowlands are underlain by clay, while 
the slopes on both sides of the valley are composed of coarser tex- 
tured deposits that extend to the base of the mountains. Canals, 
fed either from Sevier River or San Pitch Creek, supply the lower 
part of the valley, which locally is so wet as to need drainage; but 
above the ditches desert conditions prevail. 

Ground water lies within 50 feet of the surface in a considerable 
area in this part of the valley, and a number of wells have been sunk 
here. West of Gunnison, near the river, there are many flowing 
wells that average only 30 feet in depth. The water occurs in gravel 
beneath about 25 feet of clay, and the wells, which are 2 inches in 
diameter, flow about 50 gallons a minute under a pressure at the 
surface of about 1 pound. 

Farther up the valley, in the vicinity of Axtel, about 1 mile east of 
the river, there is a group of dug wells that average 60 feet in depth. 
The deepest bore hole in this part of the valley is 1^ inches in diame- 
ter and 200 feet deep (No. 109 on the map). In this well alkaline 
water is found in sand at a depth of 45 feet, below which between 



DETAILED DESCRIPTIONS. 43 

160 and 200 feet of alternating beds of sand and gravel, separated by 
clay, were encountered, which yielded a better quality of water that 
rose within 26 feet of the surface. Although the strata of the valley 
range dip toward the river, the catchment area is small, the rocks are 
chiefly fine-textured shales and limestones, and the opportunities for 
absorption and transmission are poor. On the east side of the valley 
the conditions are worse, for the little water that is contained in the 
gypsiferous shales is strongly impregnated with dissolved salts. 

The town of Gunnison is situated at the southern end of the Gun- 
nison Plateau, near the mouth of San Pitch Creek. A fair amount of 
water is furnished by canals, but there is urgent need for a supply of 
pure drinking water. There are a few shallow wells which derive 
their supply largely from the seepage of the canals. The w^ater level 
in these wells fluctuates about 10 feet a year, being highest in the 
midst of the irrigation season. South of Gunnison a number of wells, 
less than 50 feet deep, have been sunk into the valley deposits, in 
which water is found in gravel beneath the surface cover of clay. 
The supply is derived largely from the seepage from the canals, 
and the quality of the water is only fair. No deep wells have been 
sunk in this part of the valley, and although the elevation is so high 
that flowing wells can hardly be expected, it is likely that a better 
quality can be obtained beneath the upper waters, and a test should be 
made. Probably the most satisfactory domestic supply for Gunnison 
is obtainable from springs at the base of the Wasatch Plateau north 
of Mayfield, presently to be described. 

MAYFIELD AND VICINITY. 

Mayfield is situated On Twelvemile Creek where it emerges from 
its canyon in the Wasatch Plateau, in a narrow lowland known as 
Arapien Valley, that trends north-south along a fault. On the west 
is a range of hills composed of eastward-dipping gypsiferous shales, 
and on the east is the dip slope of the Wasatch monocline. Maj^field 
and Arapien Valley are watered by ditches that tap Tw^elvemile 
Creek at the mouth of its canyon. A spring near the bed of the creek 
about 1 mile above town may be utilized as a source of domestic 
supply. 

A number of wells, ranging in from 45 to 60 feet, have been 
sunk in the town, but many of them go dry, or almost dry, in the 
late winter, although during the irrigation season they contain 
between 15 and 20 feet of water. The westward-dipping sandstones 
that outcrop in the uj^per valley of Twelvemile Creek may contain 
water under pressure. The conditions here are complicated by minor 
step faulting along the flanks of the monocline, but it is likel}^ that 
wells sunk near the mouth of the canyon deep enough to penetrate 



44 UNDERGROUND WATER IN VALLEYS OF UTAH. 

the overlying Wasatch beds will strike artesian water in the sand- 
stone. 

In the hilly faulted zone between Mayfield and Manti the main 
supply of underground water is derived from springs, including both 
fault and seep springs, 14 of which yield more than 16 second-feet. 
These comprise both seep and fault springs. The most remarkable 
spring in this area is that in the Morrison coal mine (No. 28 on map), 
east of Sterling. Before the mine was opened the hillside at the 
entrance to the mine was dry, but in driving the tunnel through the 
eastward-dipping sandstone water was encountered, the amount in- 
creasing with the length of the workings, until a stream was developed 
which in August, 1905, discharged 5.6 second-feet. It is likely that 
the water is brought up through the fault east of the mine from the 
westward-dipping sandstone that outcrops on the Wasatch Plateau. 
The water being under hydrostatic pressure, rises when it reaches the 
fault plane, as illustrated in fig. 4, p. 26. This spring suggests the 
desirability of prospecting for similar occurrences. 

The small town of Sterling is watered by Sixmile Creek, which 
furnishes a good supply for irrigation, but the insanitary custom 
prevails of using for domestic purposes the ditch water that flows 
through the streets. The conditions can also be improved by develop- 
ing springs or by piping from the creek above the town. 

MANTI AND EPHRAIM. 

Above the narrows of San Pitch Creek the valley broadens to a 
width of 5 miles at Manti 'and becomes 8 miles wide at Ephraim, On 
the west Gunnison Plateau, which is underlain for the most part by 
Eocene strata that dip west at a low angle, rises abruptly above the 
valley along a fault. On the east low, detached hills, composed of 
westward- dipping Manti beds, lie at the base of the Wasatch mono- 
cline. Where the creeks have cut deep, small outcrops of Laramie (?) 
sandstone are exposed below the Eocene strata, which underlie the 
surface of the greater part of the monocline in this area. Water for 
irrigation is supplied by San Pitch, Ephraim, Willow, and Manti 
creeks, which are supplemented in the lowlands to a small extent by 
flowing wells. The central part of the valley between Manti and 
Ephraim is occupied by a marsh. The conditions here, however, are 
reported to have been improved since the early days of settlement by 
the diversion of the waters of San Pitch Creek for use in irrigation, 
and considerable areas have been reclaimed. 

Ground water lies within 10 feet of the surface in a large area in 
the central part of the valley, where many wells have been driven, 
but toward the mountains water lies deeper and there are only a few 
dug wells. Most of the wells in the lowlands are 1^ or 2 inches in 



DETAILED DESCRIPTIONS. 45 

diameter and between 125 and eSOO feet in depth. Judging by the 
imperfect records, there is little uniformity in the distribution of the 
deposits, which appear to be lenticular masses of gravel, sand, and 
clay. A typical section is afforded by the following log : 

Log of R. Taylor iccll, in SW. i sec. 33, T. 15 S., R. 3 E. (I\'o. 190 on p. J5.) 



Thick- 
ness. 



Depth. 



Clay with streaks of gravel 

Clay 

Sand and gravel 

Clay and sand 

Gravel 



25 
115 



145 



25 
140 
146 
291 
29 i 



In this well the first flow was obtained at 140 feet, and a stronger 
flow^, amounting to 28 gallons a minute under a pressure of 5 pounds 
at the surface, was encountered in the lowest gravel. Most of the 
Avells in this area do not go beyond the first flow, which is commonly 
reached at a depth of about 125 feet, but in some wells as many as 
six flows are encountered between 125 and 300 feet. The flow of all 
the wells in this vicinity varies more or less with the season, and the 
yield of the shallower ones particularly is greater in summer than 
in winter. It is also found that the sinking of a new well in an area 
where wells are close together frequentl}^ interferes with the flow 
of the old ones. On the eastern side of the valley, whence the main 
supply is derived, the wells are better and more gravel is reported. 
It is desirable in this region to drive a deep well to test conditions 
and to sink more wells of larger bore to the lower horizons to obtain 
increased flow^s. In order to ascertain conditions concerning the 
available supply for pumping, experimental wells should also be put 
down outside of the area where flows are obtained. It is probable 
also that deep wells sunk near the base of the mountains on the east 
side of the valley will strike water under pressure in the Laramie 
sandstone, but the absorption area here is not so large as that farther 
north. 

Manti is built on the alluvial fan of Manti Creek, which is the chief 
source of Avater supply. The toAvn is underlain by coarse gravel in 
which are few Avells, the deepest having been sunk about 100 feet, and 
very little water is reported to have been found. Manti is one of the 
few towns in this area that are provided with waterworks. Seep 
springs in the mountains on the south side of the creek have been 
developed, whence the water is piped to the city, and furnish a good 
supply. 

Ephraim, situated on the alluvial slope about 2 miles below the 
mouth of the canyon of Ephraim Creek, is supplied with water for 
domestic purposes by a number of wells, the depth of which increases 
with the surface elevation. The wells in the lower part of town are 



46 UNDERGROUND WATER IN VALLEYS OF UTAH. 

only 30 feet deep, but those farther east are 90 feet. In the upper 
outskirts there are no wells, and the people depend on the ditches for 
water. A few years ago a well 2 inches in diameter and 440 feet 
deep was sunk near the town hall in search of flowing water. At 
160 feet water was found which rose to IT feet below the surface, and 
at 340 feet water stood in the pipe 60 feet below the ground. It is 
reported that the lower 100 feet of the drilling was through bed rock. 
A considerable part of the town appears to be underlain to a depth 
of from 10 to 20 feet by clay, which overlies water-bearing sand and 
gravel. The water is therefore protected to a certain extent from 
contamination, but a better supply is available in springs a few miles 
up Ephraim Canyon. 

MORONI AND VICINITY. 

Between Ephraim and Moroni the conditions are similar to those 
farther south. A number of flowing wells have been obtained in the 
lowlands, while the uplands remain to a large extent undeveloped. 
Some of the best wells in the area under consideration are located 
here. Most of them are 2 inches in diameter and about 130 feet deep, 
and discharge from 10 to 30 gallons a minute; but a well in NW. J 
sec. 9, T. 16 S., R. 3 E., belonging to Joseph Seely, is exceptional in 
character. This well is 4 inches in diameter and 344 feet deep and 
yields 160 gallons a minute under a pressure of 6 pounds at the sur- 
face. An approximate record of this well is as follows: 

Approximate record of ivell Wo. 205, in feet. 



Depth. 



Thick- 
ness. 



Clay / 

Sand with streaks of clav 

Clay ■ 

Sand 

Alternating layers of gravel, sand, and clay 



15 

80 

130 

150 

344 



15 
65 
50 
20 
194 



Several flows were obtained between 130 and 344 feet, but the best 
one occurred at the latter depth, in a bed of gravel 10 feet thick. In 
one well the drill was sunk 300 feet deeper, through clay all the way. 
These results will probably encourage the sinking of other wells in 
this vicinity. The extent of the area in which these conditions pre- 
vail can be determined only by testing, but it may be conjectured 
that they persist at least over several square miles. 

The town of Moroni is situated at the southern end of the high- 
land between the two forks of Sanpete Valley. Canals fed by San 
Pitch Creek form its chief source of water supply, but the town is 
poorly provided with water for domestic purposes. There are a 
number of dug wells, ranging in depth from 10 to 60 feet. The qual- 



DETAILED DESCRIPTIONS. 47 

ity of the water, however, is impaired by seepage from the upper 
canal. Probably the springs on the west side of the valley (p. 103) 
are the most desirable source of water for the domestic supply of 
Moroni. 

FOUNTAIN GREEN AND WALES. 

The broad western fork of Sanpete Valley is bordered on the east 
by a low, barren ridge, underlain by Eocene shales and limestones 
and capped by lava flows, and is limited on the west by the high and 
narrow Gunnison Plateau. The northern end of the plateau is 
underlain by beds of sandstone and conglomerate, which lie almost 
flat or dip westward at a low angle, while farther south these beds 
are capped by shales and limestones, and along the eastern border 
steep-lying, eastward-dipping beds of sandstone and conglomerate 
mark the presence of a fault. Toward the northwest the valley 
narrows, and about 4 miles above Fountain Green terminates at 
the debris- covered divide between Sanpete and Salt Creek valleys. 
No perennial streams are fed by the run-off in this area, but a remark- 
able series of springs issue along the base of Gunnison Plateau. 

Between Moroni and Fountain Green, ground water lies within 10 
feet of the surface in a narrow belt, above which it lies at greater 
depths, as shown on the map (PI. VI). In this region there are a 
few flowing wells and a number of pumping ones, but the main water 
supply is derived from springs. 

Within a distance of 10 miles between Wales and Fountain Green, 
associated with the fault at the base of Gunnison Plateau, there are 
seven springs, the aggregate yield of which amounts to 15.9 second- 
feet. These springs have many features in common. Their tem- 
perature is about the same, approximating the mean annual tem- 
perature of the region; the water of all contains abundant calcium 
carbonate, which is deposited as tufa; and the flow, except that of 
one spring, is reported not to vary. The discharge of these springs 
is not affected by heavy showers, and in view of the small tributary 
drainage area and the scarcity of limestone, a distant though un- 
known source is indicated. Possibly the water is derived from the 
westward-dipping sandstone that outcrops on the Wasatch Plateau 
and probably underlies the valley. This chance suggests the desir- 
ability of sinking a deep well in the valley in search of artesian water 
from bed rock (pp. 22-23) . The dip of the sandstone may flatten out, 
for the low temperature of the springs does not imply a deep-seated 
source, but the depth to the water-bearing beds can not be predicted. 

It is reported that the flow of one of these springs (No. YO on map) 
was increased fivefold by driving a tunnel through debris to bed rock. 
This, together with the general facts of occurrence, suggest that 
prospecting might profitably be undertaken along the fault line with 



48 UNDERGEOUND WATER IN VALLEYS OF UTAH. 

the idea of increasing present supplies and of developing new 
ones. 

Another point should be mentioned. The springs are separated 
from the settlements by a mile or more of sand and gravel, in which 
loss occurs by absorption, although aeration of the water causes the 
precipitation of calcium carbonate, which tends to seal the channels, 
especially in their upper part. Much of this loss could be prevented 
by using pipes instead of ditches. 

Wales is situated on the alluvial slope near the base of the plateau 
and is supplied with water principally from Wales Greek and from 
springs northwest of the town. There are a few wells in Wales, 
ranging from 30 to 90 feet in depth, and the fields below the town 
are irrigated from a reservoir below Moroni. The quality of the 
domestic supply can be much improved by using pipes instead of 
open ditches to convey water from the springs. 

The small toAvn of Freedom is noteworthy as being one of the few 
settlements in the area under consideration that have public water 
S3^stems. The flow of Current Spring, amounting to about 1 second- 
foot, is distributed through pipes and furnishes a very satisfactory 
supply. 

Fountain Green is suppled almost entirely by the large spring at 
the base of the plateau about a mile and a half west of the town. (PI. 
IV, A.) The yield of this spring, as measured by G. S. Jarvis in 
September, 1905, amounted to 12.4 second-feet. It is reported that 
the winter discharge falls off perceptibly, but figures to verify this 
report are not available. The domestic supply would be bettered in 
quality if the water were distributed in pipes instead of open ditches. 

There are a number of dug wells in and about Fountain Green, 
ranging from 10 to 50 feet in depth ; and about 1896 the town sank a 
2-inch well to a depth of 285 feet, the log of which is given below : 

Log of ivell at Fountain Green, No. 218. 



Thick- 
ness. 



Depth. 



Gravel 

Alternate beds of clay,.sand, and gravel 

Clay 

Sand 

Clay 



15 
113 
200 
260 
285 



MOUNT PLEASANT AND VICINITY. 

The eastern fork of Sanpete Valley is occupied by the headwaters 
of San Pitch Greek. On the west the low hills that separate the two 
forks are underlain by Eocene shales and limestones that dip west- 
Avard at a low angle and are locally capped by lava, and on the east 
the Wasatch Plateau towers above the valley. In this part of the 



DETAILED DESCRIPTIONS. 49 

plateau the summits and most of the western flank are formed of 
Laramie ( ? ) sandstone, and Eocene strata outcrop on the lower 
slopes. Here, as farther south, the monocline is Avell developed, and 
the rocks that cap the plateau dip beneath the valley filling. Spring 
City, Mount Pleasant, Fairview, and Milburn are situated on the 
east side of the valley, and their water supply is derived from the 
main creek and its branches, supplemented by a number of wells and 
springs. 

The central part of the valley is occupied by a narrow belt in 
w^hich ground water lies within 10 feet of the surface. Above the 
lowlands the surface rises to the base of the mountains at a rate of 
slightly over 100 feet a mile. The upper portion of this slope, above 
the canals, is a sagebrush-covered desert, beneath which ground 
water lies at a considerable but unknown depth. 

The wells in the lowland are chiefly shallow dug ones, possessing 
no unusual features, and the main supply of underground water is 
derived from springs. These are situated in low meadows adjacent 
to creeks and are all seep springs, of which there are several groups 
in this portion of the valley. An important group includes those 
belonging to the sugar company, located about 3 miles east of Moroni ^ 
adjacent to Cedar Creek, which in all discharge 3.8 second-feet. An- 
other group, about 2 miles northeast of these, flows 2J second-feet. 
Above Mount Pleasant, adjacent to San Pitch Creek, there are num- 
erous seeps, and in the vicinity of Fairview the total discharge of 
springs, determined by gaging the creek above and below the town 
in September, 1905, amounted to 12 second- feet. 

The Madsen and Seely tunnel, about half a mile west of the rail- 
road station at Mount Pleasant, affords an instructive example of 
the successful development of a spring. There the flow of a small 
seep has been increased several fold by tunneling, and the experiment 
might be repeated elesewhere to advantage. (See p. 28.) 

The extensive outcrop of sandstone on the crest and flanks of the 
Wasatch Plateau east of upper Sanpete Valley affords an excellent 
opportunity for absorption, and the westward dip and capping of 
Wasatch beds at the base of the plateau are favorable for obtaining 
water under pressure in wells sunk into the sandstone. These con- 
ditions are well developed between Spring City and Milburn. If 
results are favorable, it is likely that flows can be obtained well up 
on the barren slopes toward the base of the mountains. 

Spring City is situated near the base of a long alluvial slope in an 

embayment that is partly separated from the main valley by a low 

ridge of westward-dipping Manti beds. The main water supply is 

obtained from ditches fed by Canal and Oak creeks, supplemented 

iRR 199—07 M 4 



50 UNDERGROUND WATER IN VALLEYS OF UTAH. 

by springs and wells. Ground water lies within 10 feet of the sur- 
face in a narrow stip adjoining the lower part of the town, but in 
the upper part the depth to water increases to 50 feet or more. 
There are a few flowing wells in the valley deposits southwest of 
Spring City. Wells Nos. 194 and 195 are 2 inches in diameter, 200 
feet deep, and yield an average flow of 20 gallons a minute under 
a- pressure of 3| pounds at the surface. A feeble first flow was ob- 
tained at 150 feet and the main flow at 200 feet. Similar results can 
doubtless be obtained in other wells. There are a number of seep 
springs in and near the town, the discharge of which ranges between 
4 and 44 gallons a minute. It is likely that the yield can be increased 
and other springs developed by tunneling. 

Mount Pleasant, located on the alluvial slope about midway be- 
tween San Pitch and the base of the mountains, has lately in- 
stalled public waterworks. Water is diverted from Pleasant Creek 
near the mouth of its canyon and flumed to a reservoir, whence it is 
distributed throughout the town. The success of this project shows 
what can be accomplished at small cost by most of the settlements 
in Sanpete and Sevier valleys. The depth to ground water ranges 
from 10 feet in the lower part to more than 100 feet in the upper 
part of the town. Approximate measurements show that the slope of 
the ground-water surface is less than that of the ground, the figures 
being respectively 95 and 170 feet in a mile. The annual fluctuation 
of the ground-water surface between summer maximum and winter 
minimum is reported to average about 10 feet. 

Fairview and Milburn are situated near San Pitch Creek, at the 
base of the alluvial slope. In the lower part of the towns ground 
water lies near the surface, and swampy places exist, while on the 
upper slopes depth to water is considerably over 50 feet. Springs 
can be developed in this vicinity, and it is desirable that a deep test 
well should be sunk in the lower part of the valley. 



WELL DATA. 



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meadow, 
foothills. 

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UNDERGEOUI^D WATER IN VALLEYS OF UTAH. 



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INDEX 



A. Page. 

Alluvial fan, view of 5 

Annabelle, water supplies at - 39 

Asimina eocenica Lesq., occurrence of 9 

Aurora, water supplies at 41 

Axtel, wells near 42-43 

B. 

Bed rocks, occurrence and character of. 8-12 

water in 22-23 

recovery of 25-27 

Black Knoll Springs, character of 39 

C. 

Canal Creek, flow of 17 

Canals, flow of 20-21 

supply of 17 

Cedar Creek, flow of 17 

Cedar Ridge Creek, flow of 20 

Clear Creek, flow of 17, 20 

Climate, character of 5 

Colorado rocks, occurrence and character of. 9 

Cope, E. D., on the Manti beds 11 

Corn Creek, rocks on 10 

Cottonwood Creek, flow of 17, 20 

Cove Creek, flow of 20 

Cretaceous rocks, occurrence and character 

of 9-10 

Crops, character of 5 

Current Spring, flow of 48 

D. 

Dams, subsurface, recovery of water by 30 

Dry Creek, water of, analysis of 31 

E. 

Elsinore, water supplies near 35-36 

Eocene rocks, occurrence and character of. 9, 10-12 

Ephraim, water supplies at 45-46 

Ephraim Creek, flow of 17, 19 

seepage from 19 

F. 

Fairview, water supplies near 49, 50 

Fault springs, flow of 25 

occurrence of 35-50 

structure at, section showing 26 

view of 14 

Faults, occurrence and character of 13-14 

Fountain Green, springs near, description 

of 47-48 

springs near, temperature of 25 

view of 14 

water of, analysis of 31 



Page. 
Fountain Green, water supplies near 47-48 

well at, record of 48 

Freedom, alluvial fan near, view of 5 

water supply of 48 

G. 
Geology, account of 8-14 

map showing Pocket. 

Gienwood, description of 39 

Glenwood Springs, description of 39 

water of, analysis of 31 

Goniobasis, occurrence of 10 

Gunnison, flow near 18 

water supplies near , 42-43 

Gunnison Plateau, description of 7 

rocks of 10 

section on 11 

H. 

Herrins Hole Springs, character of 39 

I. 

Igneous rocks, occurrence and character of. 12 

Inoceramus labiatus, occurrence of 9 

Inverury, water resources of 39 

Irrigation, methods of, crudeness of 33 

J. 

Jarvis, C. S., work of 5, 17, 19 

Joseph, water supplies near 34-35 

Joseph Hot Springs, description of 35 

temperature of 25, 35 

J urassic rocks, occurrence and character of. 8-9 

K. 

Knowlton, F. H., fossils determined by 9 

L. 

Laramie formation, occurrence of 9-10, 22 

water in 1 22 

Lost Creek, flow of ■ 17, 20 

M. 

Madsen and Seely tunnel, spring in 49 

Manti, precipitation at 16 

water supplies at 44-45 

well near, record of 45 

Manti beds, occurrence of 11-12 

Manti Creek, flow of 17 

water of, analysis of 30 

view of 14 

Map of Utah, showing location of valleys.. . 6 
Map, geologic, of Sanpete and central Sevier 

valleys Pocket. 

61 



62 



INDEX. 



Page. 
Map, underground water, in Sanpete Valley. 24 

in central Sevier Valley 22 

Mayfield, water resources near 43-44 

Milburn, water supplies near 49, 50 

Monroe, water supplies near 36-37 

Monroe Creek, flow of 17, 20 

water of, analysis of 31 

Monroe Hot Springs, description of 36-37 

temperature of 25, 37 

water of, analysis of 37 

Monroe Peak, elevation of 7 

Moroni, water supplies near 46-47 

well near, record of 46 

Moroni canal, flow of 19 

seepage from 19 

Morrison Tunnel Spring, structure at, sec- 
tion showing 26, 44 

water of, analysis cf 31 

Mormons, settlement by 5 

Mount Pleasant, precipitation at 16 

water supplies near 48-50 

N. 

Nebo, Mount, rocks on 10 

Ninemile Spring, water of, analysis of 31 

North Creek, flow of 17 

O. 

Oak Creek, flow of 17,19 

seepage from 19 

P. 

Pavant Mountains, description of 8 

rocks of 10, 22, 23 

Physa, occurrence of 10 

Planorbis, occurrence of 10 

Pleasant Creek, flow of 17 

water of, analysis of 30 

Precipitation, amount of 15-16 

disposal of 14-15 

R. 

Rainfall. See Precipitation. 

Redbutte Creek, flow of 20 

Redmond, water supplies of 42 

well near, record of 42 

Reservoirs, recommendation for 32-33 

Richfield, precipitation at 15 

water supplies near 37-39 

well near, water of, analysis of 38 

Richfield Spring, description of 38-39 

structure at, section showing 26 

temperature of 25 

water of, analysis of 31 

S. 

Sabal, occurrence of 9 

Sabalites grayanus, occurrence of 9 

Salina, description of 41 

water supplies near 40-42 

well at, record of 41 

Salina Creek, artesian wells on 40 

flow of 17, 20 

water of, analyses of 30-31 

Salix sp., occurrence of 9 



Page. 

San Pitch Creek, character of 16 

flow of 18,21 

irrigation from 5 

tributaries of 7 

water of, analyses of 30 

See also Sanpete Valley. 

Sanpete Valley, geology of 8-14 

geology of, map showing Pocket. 

location of 5 

sections across, figures showing 12, 13 

springs in, data on 42-50, 58-60 

topography of 6-8 

underground water in 14-34 

depth to, map showing 24 

water resources in 14-34 

wells in, data on 42-50, 53-57 

Seep springs, occurrence of 27-28 

Seepage, gain and loss by 19-21 

Sevier Plateau, description of 7 

Sevier River, canals from 5 

character of 16 

flow of 17, 18-21 

seepage on 19-21 

tributaries of 6-7 

water of, analysis of 30 

Sevier Valley, geology of 8-14 

geology of, map showing Pocket. 

-location of 5, 7-8 

sections across, plate showing 12 

springs in, data on 35-44, 58 

topography of 6-8 

underground water in 14-34 

depth to, map showing 22 

water resources in 34-44 

wells in, data on 34-44, 51-54 

Sixmile Creek, flow of 17 

water of, analysis of 30 

Sphaerium, occurrence of 10 

Spring City, water supplies near 49-50 

Spring Creek, flow of 20 

Springs, flow of 21, 25-26, 27-28 

list of 58-60 

location of, maps showing 22, 24 

occurrence of 35-50 

structure at, figure showing 26 

Sterling, rocks near 9, 10 

water supplies of 44 

Streams, character of 16-17 

flow of 16-21 

water of, analyses of 30-32 

Structure, character of 13-14 

section showing 13 

T. 

Tanner, Caleb, cooperation of 5 

flow measurements by 19 

Tertiary rocks, occurrence and character of. 10-12 

Thompsons Creek, flow of 20 

Topography, description of 6-8 

Tunnels, recovery of water by 26-27, 28, 44, 49 

recovery of water by, figures showing. . 26, 28 
Twelvemile Creek, flow of 17 

water of, analysis of 30 

Twin Creek, flow of 17, 19 

seepage from 19 



INDEX. 



63 



U. Page. 

Underground water. See Water, under- 
ground. 
Utah, map of, showing location of valleys. . 6 

V. 

Valley deposits, occurrence and character of 12-13 

water in 23-24 

recovery of 27-30 

Valley Mountains, description of 8 

Vi vipara, occurrence of 10 

W. 

Wales, section near 11 

water supplies near 48 

Wasatch Plateau, description of 7 

rocks of 10, 22 

view of 14 

Water, conservation of 32-34 



Page 

Water, quality of 30-32 

Water, underground, depth to, maps show- 
ing 22, 24 

distribution of • 21-24 

pollution of 32 

quality of 31-32 

recovery of 24-30 

source of 14-21 

Water Canyon Creek, flow of 20 

Wells, list of 51-57 

location of, maps showing 22, 24 

use of 28-29, 34-50 

water of, analyses of , 31 

Wells, flowing, list of 52-56 

occurrence of 27, 29, 37-38, 40 

prospects for 27, 40 

use of 34 

water of, analyses of 31 

Willow Creek, flow of 17,21 



CLASSIFICATION OF THE PUBLICATIONS OF THE UNITED STATES GEOLOGICAL 

SURVEY. 

[Water-Supply Paper No. 199.] 

The publications of the United States Geological Surve}^ consist of (1) Annual 
'Reports, (2) Monographs, (3) Professional Papers, (4) Bulletins, (5) Mineral 
Resources, (6) Water-Supply and Irrigation Papers, (7) Topographic Atlas of United 
States — folios and separate sheets thereof, (8) Geologic Atlas of United States — folios 
thereof. The classes numbered 2, 7, and 8 are sold at cost of publication; the others 
are distributed free. A circular giving complete lists can be had on application. 

Most of the' above publications can be obtained or consulted in the following ways: 

1. A limited number are delivered to the Director of the Survey, from whom they 
can be obtained, free of charge (except classes 2, 7, and 8), on application. 

2. A certain number are delivered to Senators and Representatives in Congress for 
distribution. , 

3. Other copies are deposited with the Superintendent of Documents, Washington, 
D. C., from whom they can be had at prices slightly above cost. 

4. Copies of all Government publications are furnished to the principal public 
libraries in the large cities throughout the United States, where they can be consulted 
by those interested. 

The Professional Papers, Bulletins, and Water-Supply Papers treat of a variety of 
subjects, and the total number issued is large. They have therefore been classified 
into the following series: A, Economic geology; B, Descriptive geology; C, System- 
atic geology and paleontology; D, Petrography and mineralogy; E, Chemistry and 
physics; F, Geography; G, Miscellaneous; H, Forestry; I, Irrigation; J, Water stor- 
age; K, Pumping water; L, Quality of water; M, General hydrographic investiga- 
tions; N, Water power; O, Underground waters; P, Hydrographic progress reports. 
This paper is the one hundred and seventeenth in Series B and the seventieth in 
Series O, the complete lists of which follow (PP= Professional Paper; B=Bulletin; 
WS=Water-Supply Paper): 

SERIES B, DESCRIPTIVE GEOLOGY. 

B 23. Observations on the junction between the Eastern sandstone and the Keweenaw series on 

Keweenaw Point, Lake Superior, by R. D. Irving and T. C. Chamberlin. 1885. 124 pp., 17 

pis. (Out of stock.) 
B 33. Notes on geology of northern California, by J. S. Diller. 1886. 23 pp. (Out of stock.) 
B 39. The upper beaches and deltas of Glacial Lake Agassiz, by Warren Upham. 1887. 81 pp., 1 pi. 

(Out of stock.) 
B 40. Changes in river courses in Washington Territory due to glaciation, by Bailey Willis. 1887. 

10 pp., 4 pis. (Out of stock.) 
B 45. The present condition of knowledge of the geology of Texas, by R. T. Hill. 1887. 94 pp. (Out 

of stock.) 
B 53. The geology of Nantucket, by N. S. Shaler. 1889. 55 pp., 10 pis. (Out of stock. ) 
B 57. A geological reconnaissance in southwestern Kansas, by Robert Hay. 1890. 49 pp., 2 pis. 
B 58. The glacial boundary in western Pennsylvania, Ohio, Kentucky, Indiana, and Illinois, by G. F. 

Wright, with introduction by T. C. Chamberlin. 1890. 112 pp., 8 pis. (Out of stock. ) 
B 67. The relations of the traps of the Newark system in the New Jersey region, by N. H. Darton. 

1890. 82 pp. (Out of stock.) 
B 104. Glaciation of the Yellowstone Valley north of the Park, by W. H. Weed. 1893. 41 pp., 4 pis. 

iRR 199—07 5 I 



II SERIES LIST. 

B 108. A geological reconnaissance in central Washington, by I. C. Russell. 1893. 108 pp., 12 pis. 

(Out of stock.) 
B 119. A geological reconnaissance in northwest Wyoming, by G. H. Eldridge. 1894. 72 pp., 4 pis. 
B 137. The geology of the Fort Riley Military Reservation and vicinity, Kansas, by Robert Hay. 1896. 

35 pp., 8 pis. 
B 144. The moraines of the Missouri Coteau and their attendant deposits, by J. E. Todd. 1896. 71 

pp., 21 pis. 
B 158. The moraines of southeastern South Dakota and their attendant deposits, by J. E. Todd. 1899. 

171pp., 27 pis. 
B 159. The geology of eastern Berkshire County, Massachusetts, by B. K. Emerson. 1899. 139 pp., 

9 pis. 
B 165. Contributions to the geology of Maine, by H. S. Williams and H. E. Gregory. 1900. 212 pp., 

14 pis. 
WS 70. Geology and water resources of the Patrick and Goshen Hole quadrangles in eastern Wyoming 

and western Nebraska, by G. I. Adams. 1902. 50 pp:, 11 pis. 
B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell. 1902. 192 

pp., 25 pis. 
PP 1. Preliminary report on the Ketchikan mining district, Alaska, with an introductory sketch of 

the geology of southeastern Alaska, by A. H. Brooks. 1902. 120 pp., 2 pis. 
PP 2. Reconnaissance of the northwestern portion of Seward Peninsula, Alaska, by A. J. Collier. 

1902. 70 pp., 11 pis. 
PP 3. Geology and petrography of Crater Lake National Park, by J. S. Diller and H. B. Patton. 1902. 

167 pp., 19 pis. 

PP 10. Reconnaissance from Fort Hamlin to Kotzebue Sound, Alaska, byway of Dall, Kanuti, Allen, 
and Kowak rivers, by W. C. Mendenhall. 1902. 68 pp., 10 pis. 

PP 11. Clays of the United States east of the Mississippi River, by Heinrich Ries. 1903. 298 pp., 9 pis. 
(Out of stock.) 

PP 12. Geology of the Globe copper district, Arizona, by F. L. Ransome. 1903. 168 pp., 27 pis. 

PP 13. Drainage modifications in southeastern Ohio and adjacent parts of West Virginia and Ken- 
tucky, by W. G. Tight. 1903. Ill pp., 17 pis. (Out of stock.) 

B 208. Descriptive geology of Nevada south of the fortieth parallel and adjacent portions of Cali- 
fornia, by J. E. Spurr. 1903. 229 pp., 8 pis. (Out of stock.) 

B 209. Geology of Ascutney Mountain, Vermont, by R. A. Daly. 1903. 122 pp., 7 pis. 

WS 78. Preliminary report on artesian basins in southwestern Idaho and southeastern Oregon, by 
I.C.Russell. 1903. 51 pp., 2 pis. 

PP 15. Mineral resources of the Mount Wrangell district, Alaska, by W. C. Mendenhall and F. C. 
Schrader. 1903. 71 pp. 10 pis. 

PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred 
and third meridian, by N. H. Darton. 1903. 69 pp., 43 pis. 

B 217. Notes on the geology of southwestern Idaho and southeastern Oregon, by I. C. Russell. 1903. 
83 pp., 18 pis. 

B 219. The ore deposits of Tonopah, Nevada (preliminary report), by J. E. Spurr. 1903. 31 pp., 1 pi. 

PP 20. A reconnaissance in northern Alaska in 1901" by F. C. Schrader. 1904. 139 pp., 16 pis. 

PP 21. The geology and ore deposits of the Bisbee quadrangle, Arizona, by F. L. Ransome. 1904, 

168 pp., 29 pis. 

WS 90. Geology and water resources of part of the lower James River Valley, South Dakota, by J. E. 
Todd and C. M. Hall. 1904. 47 pp., 23 pis. 

PP 25. The copper deposits of the Encampment district, Wyoming, by A. C. Spencer. 1904. 107 pp., 
2 pis. (Out of stock.) 

PP 26. Economic resources of the northern Black Hills, by J. D. Irving, with contributions by S. F. 
Emmons and T. A. Jaggar, jr. 1904. 222 pp., 20 pis. 

PP 27. A geological reconnaissance across the Bitterroot Range and Clearwater Mountains in Mon- 
tana and Idaho, by Waldemar Lindgren. 1904. 122 pp., 15 pis. 

PP 31. Preliminary report on the geology of the Arbuckle and Wichita mountains in Indian Ter- 
ritory and Oklahoma, by J. A. Taff, with an appendix on reported ore deposits in the Wichita 
Mountains, by H. F. Bain. 1904. 97 pp., 8 pis. 

B 235. A geological reconnaissance across the Cascade Range near the forty-ninth parallel, by G. O. 
Smith and F. C. Calkins. 1904. 103 pp., 4 pis. 

B 236. The Porcupine placer district, Alaska, by C. W. Wright. 1904. 35 pp., 10 pis. 

B 237. Igneous rocks of the Highwood Mountains, Montana, by L. V. Pirsson. 1904. 208 pp., 7 pis. 

B 238. Economic geology of the lola quadrangle, Kansas, by G. I. Adams, Erasmus Haworth, and 
W. R. Crane. 1904. 83 pp., 1 pi. 

PP 32. Geology and underground water resources of the central Great Plains, by N. H. Darton. 1905. 
433 pp., 72 pis. 

WS 110. Contributions to hydrology of eastern United States, 1904; M. L. Fuller, geologist in charge. 
1905. 211 pp., 5 pis. 



SERIES LIST. Ill 

B 242. Geology of the Hudson Valley between the Hoosic and the Kinderhook, by T. Nelson Dale. 

1904. 63 pp., 3 pis. 

PP 34. The Delavan lobe of the Lake Michigan glacier of the Wisconsin stage of glaciation and 

associated phenomena, by W. C. Alden. 1904. 106 pp., 15 pis. 
PP 35. Geology of the Perry Basin in southeastern Maine, by G. O. Smith and David White. 1905. 

107 pp., 6 pis. 
B 243. Cement materials and industry of the United States, by E. C. Eckel. 1905. 395 i)p., 15 pis. 
B 246. Zinc and lead deposits of northeastern Illinois, by H. F. Bain. 1904. 56 pp., 5 pis. 
B 247. The Fairhaven gold placers of Seward Peninsula, Alaska, by F. H. Moffit. 1905. 85 pp., 14 pig. 
B 249. Limestones of southwestern Pennsylvania, by F. G. Clapp. 1905. 52 pp., 7 pis. 
B 250. The petroleum fields of the Pacific coast of Alaska, with an account of the Bering River coal 

deposit, by G. C. Martin. 1905. 65 pp., 7 pis. 
B 251. The gold placers of the Fortymile, Birch Creek, and Fairbanks regions, Alaska, by L. M. 

Prindle. 1905. 16 pp., 16 pis. 
WS 118. Geology and Avater resources of a portion of east-central Washington, by F. C. Calkins. 1905. 

96 pp., 4 pis. 
B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell. 

1905. 138 pp., 24 pis. 

PP 36. The lead, zinc, and fluorspar deposits of western Kentucky, by E. O. Ulrich and W. S. Tangier 

Smith. 1905. 218 pp., 15 pis. 
PP 38. Economic geology of the Bingham mining district of Utah, by J. M. Boutwell, with a chapter 

on areal geology, by Arthur Keith, and an introduction on general geology, by S. F. Emmons. 

1905. 413 pp., 49 pis. 
PP 41. The geology of the central Copper River region, Alaska, by W. C. Mendenhall. 1905. 133 pp., 

20 pis. 
B 254. Report of progress in the geological resurvey of the Cripple Creek district, Colorado, by 

Waldemar Lindgren and F. L. Ransome. 1904. 36 pp. 
B 255. The fluorspar deposits of southern Illinois, by H. Foster Bain. 1905. 75 pp., 6 pis. (Out of 

stock.) 
B 256. Mineral resources of the Elders Ridge quadrangle, Pennsylvania, by R. W. Stone. 1905. 

85 pp., 12 pis. 
B 257. Geology and paleontology of the Judith River beds, by T. W. Stanton and J. B. Hatcher, with 

a chapter on the fossil plants, by F. H. Knowlton. 1905. 174 pp., 19 pis. 
PP 42. Geology of the Tonopah mining district, Nevada, by J. E. Spurr. 1905. 295 pp., 24 pis. 
WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by 

C. R. Keyes. 1905. 42 pp., 9 pis. (Out of stock.) 
WS 136. Underground Avaters of Salt River Valley, Arizona, by W. T. Lee. 1905. 194 pp., 24 pis. 
PP 43. The copper deposits of Clifton-Morenci, Arizona, by Waldemar Lindgren. 1905. 375 pp., 25 pis. 
B 265. Geology of the Boulder district, Colorado, by N. M. Fenneman. 1905. 101 pp., 5 pis. 
B 267. The copper deposits of Missouri, by H. F. Bain and E. 0. Ulrich. 1905. 52 pp., 1 pi. 
PP44. Underground Avater resources of Long Island, Ncav York, by A. C. Veatch and others. 1905. 

394 pp., 34 pis. 
WS 148. Geology and water resourc s of Oklahoma, by C. N. Gould. 1905.- 178 pp., 22 pis. 
B 270. The configuration of the rock floor of Greater New York, by W. H. Hobbs. 1905. 96 pp., 5 pis. 
B 272. Taconic physiography, by T. M. Dale. 1905. 52 pp., 14 pis. 
PP 45. The geography and geology of Alaska, a summary of existing knoAvledge, by A. H. Brooks, 

Avith a section on climate, by Cleveland Abbe, jr., and a topographic map and description 

thereof, by R. M. G.oode. 1905. 327 pp., 34 pis. 
B 273. The drumlins of southeastern Wisconsin (preliminary paper), by W.C. Alden. 1905. 46 pp., 

9 pis. 
PP 46. Geology and undergrouiid Avater resources of northern Louisiana and southern Arkansas, by 

A. C. Veatch. 1906. 422 pp., 51 pis. 
PP 49. Geology and mineral resources of part of the Cumberland Gap coal field, Kentucky, by G. H. 

Ashley and L. C. Glenn, in cooperation Avith the State Geological Department of Kentucky, 

C. J. Norwood, curator. 1906. 239 pp., 40 pis. 
PP 50. The Montana lobe of the KeeAvatin ice sheet, by F. H. H. Calhoun. 1906. 62 pp., 7 pis. 
B 277. Mineral resources of Kenai Peninsula, Alaska: Gold fields of the Turnagain Arm region, by 

F. H. Moffit; and the coal fieldsof the Kachemak Bay region, by R. W. Stone. 1906. 80pp., 

18 pis. (Out of stock.) 
WS 154. The geology and Avater resources of the eastern portion of the Panhandle of Texas, by C. N. 

Gould. 1906. 64 pp., 15 pis. 
B278. Geology and coal resources of the Cape Lisburne region, Alaska, by A. J. Collier. 1906. 54 

pp., 9 pis. (Out of stock.) 
B279. Mineral resources of the K ttanning and Rural Valley quadrangles, Pennsylvania, by Charles 

Butts. 1906. 198 pp., 11 pis. 
B 280. The Rampart gold placer region, Alaska, by L. M. Prindle and F. L. Hess. 1906. 54 pp., 7 pis. 

(Out of stock.) 



IV SERIES LIST. 

B 282. Oil fields of the Texas-Louisiana Gulf Coastal Plain, by N. M. Fenneman. 1906. 146 pp., 11 pis. 
WS 157. Underground water in the valleysof Utah Lake and Jordan River, Utah, by G. B. Richardson. 

1906. 81 pp., 9 pis. 
PP 51. Geology of the Bighorn Mountains, by N. H. Darton. 1906. 129 pp., 47 pis. 
WS 158. Preliminary report on the geology and underground waters of the Roswell artesian area, 

New Mexico, by C. A. Fisher. 1906. 29 pp., 9 pis. 
PP 52. Geology and underground waters of the Arkansas Valley in eastern Colorado, by N. H. Darton. 

1906. 90 pp., 28 pis. 
WS 159. Summary of underground-water resources of Mississippi, by A. F. Crider and L. C. Johnson. 

1906. 86 pp., 6 pis. 

PP 53. Geology and water resources of the Bighorn basin, Wyoming, by Cassius A. Fisher. 1906. 
72 pp., 16 pis. 

B 283. Geology and mineral resources of Mississippi, by A. F. Crider. 1906. 99 pp., 4 pis. 

B 286. Economic geology of the Beaver quadrangle, Pennsylvania (southern Beaver and northwest- 
ern Allegheny counties), by L. H. Woolsey. 1906. 132 pp., 8 pis. 

B 287. The Juneau gold belt, Alaska, by A. C. Spencer, and a reconnaissance of Admiralty Island, 
Alaska, by C. W. Wright. 1906. 161 pp., 37 pis. 

PP'54. The geology and gold deposits of the Cripple Creek district, Colorado, by W. Lindgren and 
F. L. Ransome. 1906. 516 pp., 29 pis. 

PP 55. Ore deposits of the Silver Peak quadrangle, Nevada, by J. E. Spurr. 1906. 174 pp., 24 pis. 

Ei289. A reconnaissance of the Matanuska coal field, Alaska, in 1905, by G. C. Martin. 1906. 86 pp., 

5 pis. 

WS 164. Underground waters of Tennessee and Kentucky west of Tennessee River and of an adjacent 

area in Illinois, by L. C. (^lenn. 1906. 173 pp., 7 pis. 
B 293. A reconnaissance of some gold and tin deposits of the southern Appalachians, by L. C. Groton, 

with notes on the Dahlohega mines, by W. Lindgren. 1906. 134 pp., 9 pis. 
B 294. Zinc and lead deposits of the upper Mississippi "Valley, by H. Foster Bain. 1906. 155pp., 16 pis. 
B 295. The Yukon-Tanana region, Alaska, description of Circle quadrangle, by L. M. Prindle. 1906. 

27 pp., 1 pi. 
B 296. Economic geology of the Independence quadrangle, Kansas, by Frank C. Schrader and 

Erasmus Haworth. 1906. 74 pp., 6 pis. 
-WS181. Geology and water resources of Owens Valley, California, by Willis T. Lee. 1906. 28 pp., 

6 pis. 

B 297. The Yampa coal field, Routt County, Colo., by N. M. Fenneman, Hoyt S. Gale, and M. R. Camp- 
bell. 1906. 96 pp., 9 pis. 

B 300. Economic geology of the Amity quadrangle in eastern Washington County, Pa., by F. G. 
Clapp. 1906. 145 pp., 8 pis. 

B 303. Preliminary account of Goldfield, Bullfrog, and other mining districts in southern Nevada, by 

F. L. Ransome; with notes on Manhattan district, by G. H. Garrey and W. H. Emmons, 

1907. 98 pp., 5 pis. 

B 304. Oil and gas fields of Greene County, Pa., by R. W. Stone and F. G. Clapp. 1907. 110 pp., 3 pis. 
WS 188. Water resources of the Rio Grande Valley in New Mexico and their development, by W. T. 

Lee. 1906. 59 pp.", 10 pis. 
B 306. Rate of recession of Niagara Falls, accompanied by a report on the survey of the crest, by 

W. Carvel Hall. 1906. 31 pp., 11 pis. 
PP 56. Geography and Geology of a portion of southwestern Wyoming, with special reference to coal 

and oil, by A. C. Veatch. 1907. —pp., 26 pis. 
B 308. A geologic reconnaissance in southwestern Nevada and eastern California, by S. H. Ball. 1907. 

218 pp., 3 pis. 
B 309. The Santa Clara Valley, Puente Hills, and Los Angeles oil districts, southern California, by 

G. H. Eldridge and Ralph Arnold. 1907. 266 pp., 41 pis. 

PP 57. Geology of the Marysville mining district, Montana, a study of igneous intrusion and contact 

metamorphism, by Joseph Barrell. 1907. 178 pp., 16 pis. 
WS. 191. The geology and water resources of the western portion of the Panhandle of Texas, by C. N. 

Gould. 1907. 70 pp., 7 pis. 
B 311. The green schists and associated granites and porphyries of Rhode Island, by B. K. Emerson 

and J. H. Perry. 1907. 74 pp., 2 pis. 
WS 195. Underground \yaters of Missouri, their geology and utlization, by Edward Shepherd. 1907. 

224 pp., 6 pis. 
WS 199. Underground water in Sanpete and central Sevier valleys, Utah, by G. B. Richardson. 1907. 

63 pp., 6 pis. 

SERIES O, UNDERGROUND WATERS. 

WS 4. A reconnaissance in southeastern Washington, by I. C. Russell. 1897. 96 pp., 7 pis. (Out of 

stock.) 
WS 6. Underground waters of southwestern Kansas, by Erasmus Haworth. 1897. 65 pp., 12 pis. 

(Out of stock.) 
WS 7. Seepage waters of northern Utah, by Samuel Fortier. 1897. 50 pp., 3 pis. (Out of stock.) 



SERIES LIST. V 

WS 12. Underground waters of southeastern Nebraska, by N. H. Darton. 1898. 56 pp., 21 pis. (Out 

of stock.) 
WS 21. Wells of northern Indiana, by Frank Leverett. 1899. 82 pp., 2 pis. (Out of stock.) 
WS 26. Wells of southern Indiana (continuation of No. 21), by Frank Leverett. 1899. 64 pp. (Out 

of stock.) 
WS 30. Water resources of the lower peninsula of Michigan, by A. C. Lane. 1899. 97 pp., 7 pis. (Out 

of stock.) 
WS 31. Lower Michigan mineral waters, by A. C. Lane. 1899. 97 pp., 4 pis. (Out of stock.) 
WS 34. Geology and water resources of a portion of southeastern South Dakota, ))y J. E. Todd. 1900. 

34 pp., 19 pis. 
WS 53. Geology and water resources of Nez Perces County, Idaho, Pt. I, by I. C. Russell. 1901. 

86 pp., 10 pis. (Out of stock.) 
WS 54. Geology and water resources of Nez Perces County, Idaho, Pt. II, by I. C. Russell. 1901. 

87-141 pp. (Out of stock.) 
WS 55. Geology and water resources of a portion of Yakima County, Wash., by G. O. Smith. 1901. 

68 pp., 7 pis. (Out of stock.) 
WS57. Preliminary list of deep borings in the United States, Pt. I, by N. H. Darton. 1902. 60 pp. 

(Out of stock.) 
WS 59. Development and application of water in southern California, Pt. I, by J. B. Lippincott. 1902 

95 pp., 11 pis. (Out of stock.) 
WS 60. Development and application of water in southern California, Pt. II, by J. B. "Lippincott. 1902. 

96-140 pp. (Out of stock.) 
WS 61. Preliminary list of deep borings in the United States, Pt. II, by N. H. Darton. 1902. 67 pp. 

(Out of stock.) 
WS 67. The motions of underground waters, by C. S. Slichter. 1902. 106 pp., 8 pis. (Out of stock.) 
B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell. 1902. 192 

pp., 25 pis. 
WS 77. Water resources of Molokai, Hawaiian Islands, by Waldemar Lindgren. 1903. 62 pp., 4 pis. 
WS 78. Preliminary report on artesian basins in .southwestern Idaho and southeastern Oregon, by 

I.C.Russell. 1903. 53 pp., 2 pis. 
PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred 

and third meridian, by N. H. Darton. 1903. 69 pp., 43 pis. 
WS 90. Geology and water resources of a part of the lower James River Valley, South Dakota, by J. E. 

Todd and C. M. Hall. 1904. 47 pp., 23 pis. 
WS 101. Underground waters of southern Louisiana, by G. D. Harris, with discussions of their uses 

for water supplies and for rice irrigation, by M. L. Fuller. 1904. 98 pp., 11 pis. 
WS 102. Contributions to the hydrology of eastern United States, 1903, by M. L. Fuller. 1904. 522 pp. 
WS 104. Underground waters of Gila Valley, Arizona, by W. T. Lee. 1904. 71 pp., 5 pis. 
WS 106. Water resources of the Philadelphia district, by Florence Bascom. 1904. 75 pp., 4 pis. 
WS 110. Contributions to the hydrology of eastern United States, 1904; M. L. Fuller, geologist in charge. 

1904. 211 pp., 5 pis. 
PP 32. Geology and underground water resources of the central Great Plains, by N. H. Darton. 1904. 

433 pp., 72 pis. (Out of stock.) 
WS 111. Preliminary report on underground waters of Washington, by Henry Landes. 1904. 85 pp., 

ipl. ' 
WS 112. Underflow tests in the drainage basin of Los Angeles River, by Homer Hamlin. 1904. 55 

pp., 7 pis. 
WS 114. Underground waters of eastern United States, by M. L. Fuller, geologist in charge. 1904. 

285 pp., 18 pis. 
WS 118. Geology and water resources of east-central Washington, by F. C. Calkins. 1905. 96 pp., 

4 pis. 
B 252. Preliminary report on the geology and water resources of central Oregon, by 1. C. Russell. 

190^. 138 pp., 24 pis. 
WS 120. Bibliographic review and index of papers relating to underground waters, published by the 

United States Geological Survey, 1879-1904, by M. L. Fuller. 1905. 128 pp. 
WS 122. Relation of the law to underground waters, by D. W. Johnson. 1905. 55 pp. 
WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by C. R. 

Keyes. 1905. 42pp., 9 pis.. (Out of stock.) 
WS 136. Undergro\ind waters of the Salt River Valley, by W. T. Lee. 1905. 194 pp., 24 pis. 
B 264. Record of deep-well drilling for 1904, by M. L. Fuller, E. F. Lines, and A. C. Veatch. 1905. 

106 pp. 
PP 44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905. 

394 pp., 34 pis. 
WS 137. Development of underground waters in the eastern coastal plain region of southern Cali- 
fornia, by W. C. Mendenhall. 1905, 140 pp., 7 pis. 
WS 138. Development of underground waters in the central coastal plain region of southern Cali- 
fornia, by W. C. Mendenhall. 1905. 162 pp., 5 pis. 



VI SERIES LIST. 

WS 139. Development of underground waters in the western coastal plain region of southern Cali- 
fornia, by W. C. Mendenhall. 1905. 105 pp., 7 pis. 

WS 140. Field measurements of the rate of movement of underground waters, by C. S. Slichter. 1905. 
122 pp., 15 pis. 

WS 141. Observations on the ground waters of Rio Grande Valley, by C. S. Slichter. 1905. 83 pp., 
5 pis. 

WS 142. Hydrology of San Bernardino Valley, California, by W. C. Mendenhall. 1905. 124 pp., 13 pis. 

WS 145. Contributions to the hydrology of eastern United States; M. L. Fuller, geologist in charge. 

1905. 220 pp., 6 pis. 

WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis. 

WS 149. Preliminary list of deep borings in the United States, second edition, with additions, by 

N. H. Darton. 1905. 175 pp. 
PP 46. Geology and underground water resources of northern Louisiana and southern Arkansas, by 

A. C. Veatch. 1906. 422 pp., 51 pis. 
WS 153. The underflow in Arkansas Valley in western Kansas, by C. S. Slichter. 1906. 90 pp., 3 pis. 

(Out of stock.) 
WS 154. The geology and water resources of the eastern portion of the Panhandle of Texas, by C. N. 

Gould. 1906. 64 pp., 15 pis. 
WS 155. Fluctuations of the water level in wells, with special reference to Long Island, New York, by 

A. C. Veatch. 1906. 83 pp., 9 pis. 
WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson. 

1906. 81 pp., 9 pis. 
WS 158. Preliminary report on the geology and underground waters of the Roswell artesian area, 

New Mexico, by C. A. Fisher. 1906. 29 pp., 9 pis. 
PP 52. Geology and underground waters of the Arkansas Valley in.eastern Colorado, by N. H. Darton. 

1906. 90 pp., 28 pis. 

WS 159. Summary of underground-water resources of Mississippi, by A. F. Crider and L. C. Johnson. 

1906. 86 pp., 6 pis. 

PP 53. Geology and water resources of the Bighorn basin, Wyoming, by C. A. Fisher. 1906. 72 pp., 
16 pis. 

WS 160. Underground-water papers, 1906, by M. L. Fuller. 1906. 104 pp., 1 pi. (Out of stock.) 

WS 163. Bibliographic review and index of underground-water literature published in the United 
States in 1905, by M. L. Fuller, F. G. Clapp, and B. L. Johnson. 1906. 130 pp. 

WS 164. Underground waters of Tennessee and Kentucky west of Tennessee River and of an adja- 
cent area in Illinois, by L. C. Glenn. 1906. 17? pp., 7 pis. 

WS 181. Geology and water resources of Owens Valley, California, by W. T. Lee. 1906. 28 pp., 6 pis. 
(Out of stock.) 

WS 182. Flowing v/ells and municipal water supplies in the southern portion of the Southern Penin- 
sula of Michigan, by Frank L'everett and others. 1906. 292 pp., 5 pis. 

WS 183. Flowing wells and municipal water supplies in the middle and northern portions of the 
Southern Peninsula of Michigan, by Frank Leverett and others. 1906. 393 pp., 5 pis. 

B 298. Record of deep-well drilling for 1905, by M. L. Fuller and Samuel Sanford. 1906. 299 pp. 

WS 184. The underflow of the South Platte Valley, by C. S. Slichter and H. C. Wolff. 1906. 42 pp. 

WS 188. Water resources of the Rio Grande Valley in New Mexico and their development, by W. T. 
Lee. 1906. 59 pp., 10 pis. 

WS 190. Underground waters of Coastal Plain of Texas, by T. U. Taylor. 1907. 73 pp., 3 pis. 

WS 191. Geology and water resources of the western portion of the Panhandle of Texas, by C. N. 
Gould. 1907. 70 pp., 7 pis. 

WS 195. Underground waters of Missouri; their geology and utilization, by Edward Shepard. 

1907. 224'pp., 6 pis, 

WS 199. Underground water in Sanpete and central Sevier valleys, Utah, by G. B. Richardson. 1907 
63 pp., 6 pis. 
The following papers also relate to this subject: Underground waters of Arkansas Valley in east- 
ern Colorado, by G. K. Gilbert, in Seventeenth Annual, Pt. II; Preliminary report on artesian waters 
of a portion of the Dakotas, by N. H. Darton, in Seventeenth Annual, Pt. II; Water resources of 
Illinois, by Frank Leverett, in Seventeenth Annual, Pt. II; Water resources of Indiana and Ohio, 
by Frank Leverett, in Eighteenth Annual, Pt. IV; New developments in well boring and irrigation 
in eastern South Dakota, by N. H. Darton, in Eighteenth Annual, Pt. IV; Rock waters of Ohio, 
by Edward Orton, in Nineteenth Annual, Pt. IV; Artesian-well prospects in the Atlantic coastal 
plain region, by N. H. Darton, Bulletin No. 138. 

Correspondence should be addressed to 

The Director, ' 

United States Geological Survey, 

Washington, D. C. 
July, 1907. 

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